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CONTENTS.
3 Page.
3 Letter of transmittal RS oa oe atin ie Seipiiin'a gu Say amos Aunnse ene gale c 13
: eo ace chow en wbawesnsccbuuauene ache 15
CHAPTER I. Introductory ..--.- Se Bent ane ed Vl nbn cae ns the ai dotioas ab 17
Ba: NR era al ou gs enn cence cnc ase cimeteundigg edad 19
esis List of authors and year of Publication Sta big hae anatase a only sam een sity aes 19
pe List of papers by dates ..---..-- 22-222 seen eco ee cee eee eee cece es 22
_ CHAPTER Il. Historical review of the geologic and paleontologic work ...... 49
Bs 4 Atlantic NE TIO Fo. Oo. due Bota a cede dei cucds ann aeccubaclineies s 50
te es asia 8 aig os Cee nak xx Sal Med Sedak ccc waeken Eee 50
By se NS ee Re Cee er ero ee 56
‘A N ew Brunswick and Cape Breton...... PEE aan oaths Sod Ponienn te Aitgh Eee 59
& I pace cveu eae Se 68
* EG oa Cae abs ea bosmess~ «se lg mm a ono oct a se eowenee= ene 70
EES EL a a a 72
es ie ORRRMEOMIEY W.--:. 2... .3-a:---.-- Sendak (err SEE TS AOR NIE OES 78
& I ste eg soe SE a aw boat eens cadotndeguectage 78
-- New Brunswick and Cape Breton.:.......-..---..----- scene, wee ele
. a, GEE ea oa ato e sca sbe paciegs s5emncilaeaen cs ance ease 88
ia Se ee eae Fp siskana Pine 91
=a Northern Appalachian district. ......-......-- 222.25. cece cece ccccen ce 91
> > Granglar Quartz... ..:..-..........--- ens sawing Seeraet aan cg oe 91
IME PREM OM DIOTOOK. ode. 60 ook oe oo no ene = wane cen nne pened lec cceabaceee 96
SP OMmOnGis GALES 2.222. 28. F222 5 - ee hpi ageane togde ase seas shun peere 98
aE IRRLMGOING = oo. cane pan coe a Sees Sonn dcwenaseen~Sbetban 113
IE PROQMGURY OC o > 2 ace y= ocak wacces + se cdlament dese en bene (114
Southern Appalachian district. -....-... nance oti oid ainetat nis OR a mAs mae oe 122
a. 7 NIE SR oat Paes he oan wan cee Sc sh ieaens Ke xe qos daca nokee 122
a ‘ MSc Coed So dccs ea cace dou a Picea toes ances aa 123
: NT So oo nog ae vio dansdctas eure 124
ME 0 Ser oo cS, Fo wa ss onun mnednncase dant ouseeee 133
es Smet ete trons fun onan (aad enn ka vagt w4074eeae< annual 133
Se Moreh Caroling... ...-.------.--2-- s-----eee-s Ook ek eee 138
I TRO ONSG, os a oo oe 58 on ke penne ne anne comnee ange ucne ce 139
SI tae te ay ean © aE gt ree ee oO 144
“ I Ale ra we oo ate darn aay Ewa Sein doniemaasha eds dauWee 146
"Paleontology ea ERS oak ae ne awasa chen gine Guundae soetae keer 148
_ Northern Appalachian COG he aaah sac ka na Le heieds See 148
P eSouthern Appalachian district........---.- ..-+ .eeeecceon cea cseeess- 154
REL DOEINE OUG oe cca Osh <4 dc Pande sass a avaven oc du'ceaase cnacs 154
_ Tennessee. ........ te ee oat ree eee oy ee as ae 154
ee els wae cbe samds Aas node NG sa eS Re Login bn clnmnin ans 155
Rocky OMMCI TS SOPEEMINIOS foe ed 2k wee Sue ou nasGnccomsphoap'eélaad 155
EON CANS ore dn is 5 oma on dyna naan annus seine Gieuiswakes 155
ag “Idaho ahies ee wires PbS os cee oh So cee co eae sda cae ctw Boks sae 161
ac ete 5

: \

6 te : CONTENTS.

t

CHAPTER I]—Continued.
MONEBDD 5 osu ok bdws pone oe ednc naetacends teenene eeeee ences 2 eee ece cone
Canadian extension .... 2220 222 eee 22 ne cee none -one cone ois twinatgne
Paleontology ........ ---«- o cabenenenass cocsecchucee cust saesessaneeamemE
Interior Continental Province. ........---- Lod vewan beoen staan eneene eae
Upper Mississippi area ..-... .----+ --- 222 -- ene ee nee eee ne ences cone
WISCONSIN 222. coc ccwcdescccee cose -scce a whoo ewta ch oct ankeeeeee
Minnesota .. cco cove ccccns coc ccs cone coce cones cece sacccs cccase ane
FOWR 2c kue. Stok does mcd voeathendeaae tan tee e ekese x eces cn) a see
Lake Superior sandstone..-.....---- oypdsche ated acneand=h ooh Ann
MissOUrl . . <2 st sd cua Wis cin inet weaned yeaeeeae ee sowie tee eee
Eastern border or Adirondack sub-Province ........--- 2 ae aX
Canadian Extension. 2.6. occncavow s cock o's cs ones webn os eectdc cass Laem a
Western Border or Rocky Mountain sub-Province.......----- ---. --+-
Colorado. .wosc~- ce A Sete etry cA Ju Suticatac ke set eee
WYoming... 22. ne ncs once cece ne concen ween conc ccee sense aeab sane ee
TOG at i be oh ab ce oki eee eeeeuee wae nob aie ge Sh hate eee
Southwestern sub-Province >. 2.0.6 oso coco acdc cows nc ee saeeeeeenea’ eRe
ORAS oben aki cat ce boa dens ceisen sen potnite ane waeeen nee
Asvivons 2. Su mee iia oo iin aieiLe se ¥
Paleontology .. 030 <ler cadari cave ttn ye Sats a ace enae ale eee me
Upper Mississippi areas... os. eee ce wake a con cae deep eee he Seg I
Red sandstone of Lake Superior. ... 2.5.22. -2cc0e pecans concce coes
DnB SSS eA ite Sn Sie es ts i a eee oe Sree
Eastern border or Adirondack sub-Province................---..-----
Western border or Rocky Mountain sub-Province ..........--...-----
OSHS yes een eke en bee OEE OE ee ee ee sone
ASIGONG. <2 ses uneh po egsee os ne dre Shee an peep ae mee coe aan eeeeetee
CHAPTER III. Nomenclature employed in the description of the formations...
CD DIL BEDs s cpm ae kan Semcon Sam makin els Blew obs welen ta ee eh ee aiwend nab alors
ROROTNG 65 e woe ol sede ue whee ob een oe le BON Ola Lawn odb a nae aan

Primordial ioc o's cme Sane awa sea laen ae a ols ae oe ob es Ue > bey
Potsdam........- [NS dg tole abhi isso? ci Paige dete’ made eai So sign et ose ie ok aston Cacia as
St. Croix
Madison
Mendota

COPS OHO OSHS SHEE OH CBOK SHEESH SESH ER SHEE SEBO RHE SEER EEE EE OHSS EEE BES

PERMA DURE. 0) ae eed cpt ee bone dae same ww do adee seals areas a ae
Secret Cafion

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SSCP we CRS OTE ST OEE OEE SEEKS SEE HO OEE BREESE SOSHE SEES SEES CBSE e

Montevallo .......
Choccolocco
DN oe ace oe cera s one cw dicdwe De Cob ns ee
PPOBIO WANAGLONGS. fos 6. owe enc sh wlne ae pda Jeo ee ee Cikvoue =
Bretonian ..... . :
Acadian

ome woe wate Cee ees wees COE s Cotes Coeees S20 SS8 CE588 SEES CSeese

NPM be cd ideisee bo Sanaa oe ee |
PUD a oda Sisal ee nih a ig ek RU
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Red Benatnck. 25.5.2... -..-. 9 Eat hk ERP NE EGY a TL cp LOAN TREE EE, BE

' Erospech......-....- Pe ee se Peck. a Noh Boba dee w tee het meet nucdes
enn taatern and Western sandstone... .. 2.2.22. soe o ccne ens ce cece wece ce ncee
. SNE GEHUELOND 20 8 ooo. oy nnn dupe wales salveoc enol penwgesncy
I rose htt aon. os la. Aden ou be dawn nods bakewe tS
CHAPTER [V. Summary of the present knowledge of the formettions 5 Ro) aes 5.
IEEMIEEEIORED ETOVINGG. 20.52. os alte seen ne web tac cee ne
Fae Newfoundland and the adjoining coast of Labrador.... ......-...-...
Northwestern Newfoundland ~... 22... 2 eek ce ee en cence anne

: Eastern and Southeastern Newfoundland ...................-.2-.
Ee Neintle eee eee hte Caramel ews 5 arcana bitte woewler hula be
Seeeeerone wick and Cape breton... - 22.5.0. ons ve ccos accede couses
eis ahs(s Se.0t55 aban aoagiyah sa4 ahs Ruled dey woe ve a coe nae casdenke
New Hampshire EL ACe Soak Mea Rss ced aap he canbiralu bon « eee
Penner DEGEARLONUSOLES: 2... <-e se Seen ocwce's downers cnicd cane dccneeces
EE titania ia'e Kanan s nob qenniade es sonal aue ane a os suder oe
EME DOVANIOO os onan Jono o panens aan cesnabldee canes sane sacs ueus
"Northern Appalachian district ...-..).. 52.55... c2 0 vee c ee ace c oe bee e sean
Canadian extension -.....-. anda ee te kno le deta led af he alma 6 ao Ue oO
Somnmer™ Appalachian district’... . 2.2226 ee eee cece es wens meet ccce
ee enc SAAN dns nding Og amclen Fo ai onl bie to tate inte sek
IE is Seka sod ie tno nacwin'y LoD Ho ela ween bane maces
Gaon lala a sin wes a cGk os te ap aapiines nt eaenn a ent
ERE fo bata w ah co poeimae pede Sas knee wes «Se owe tocewan asus
RE en accye era nd lag Stn ak coco occas saaklee uoedebee

. SGT IRAE SS Sa an es ON te pa MRE WR FEE TD OY
jak Tennessee. ...--.. ee id NG Lk Seda dak = wae debe cae tee de eas
a Pere seOOCe BONMLOMOLALG. . .. 2. 5. ane toe oon wwe nsbace seccbcusesce
Rey OE MAIMUBUOIO.<'.'. o> se Sul dcicces wncedu coc cacweetelatedas

ee SA RNG pk aa NR ne eR Som
Rocky Mountain Province Bete Oty ee oa ee cee
Utah and Nevada oO Rite Se iets AER ay a eS ny ee een gaiSce de Swe
ee nS ek La selcmeak Saud Cock Cane acnw amu wnd
een Mc Enaime Gere eT oS Sean baer d od oa Sec peusdeeees

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Re mR VGNOY ii. 26/25 sys seco in set scot ovate ode ct eeee

_ Canadian extension........-.--.------- SESE pp ata lta, Us ell, Sees
PE ENIG? AM GALOGS Ys .- 5.4. 0c Lacon LacwseVacecs seuec'aceceues
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CONTENTS. ~

Section at Hemmingford.----..-.---.- De ip Javues Caen
Section at Keeseville and in Au Sable Chasm \» Bai
Rastion at Whitehall... 2.2 Veccs< eceeeecnosce Seer neee ye eked
Section at Saratoga... ... 20. sce s2st sane one, coeeeewdens woe eses SB:
Western border or Rocky Mountain sub- Pantinas Je tna eee ones, ee
Gonth Dakota 7. l..custeat a seelUp cane cs oe eee er Oe aoa fs
Wyoming {.. 22 2-.cc.s cess cat setae ph. pees beeen eee ge . ae
Colorado... j.-0s cadets eZsace ude devs ska tice as chad eae tn
_ Southwestern sub-Province ..-..... ced itiswd a wnccts code too de cde See
MY Pix hoo a Sn ths hb ca nee ene ba eee s Seelanede wale 9's Sateen 354
Apiooia =o Gn Cond nerd be Gecue ak eee 356 a
RAsUING 2i-30.0 <4 25285 Phew tee eS a ee 5s ae
Synopsis of the Cambrian group.-..-........ -.++-----+------- {nos tae ee ee
Base of Cambrian . 22a. si Sos see sae pen peo ee nas Sande ee 362 — #
Summitiof Cambrian -xdon wanemacde veo+ mone ks ene as-deel ae ae
Sedimentation of the Cambrian group...-.....-..----0- --e- cence ee ay Oe
Subdivision of the Cambrian ..... ..- 2... 5=:se¢,csaneeeeeees ae 370
Comparison with the Cambrian rocks ef other countries .-......---.-- ane ee :
HarOD6. sooo sors ct sone wane paSiun ston beeen tel a hen Tae
Seotland 3s. .oocscce tee eae Seem cduubeies ce aelekaien beens — 376
Treland \scscce.s pin cnelen woke sowed 5 nye We ob pees Sema eee ae een 377 aa
CIN spec coop ke sawsnae aces tc Ui\sece ve Uap siesw ic meiaeie ae ele eee
india ose S50 «sen pa'seae ages 12 Seb fat ee eee +1 >> Ae
Mustralla l.cs.cs specs S ciawda cokes ade sae cen ea ee 378
South Auieelca. cei ie Nee . 379
CHAPTER V. Problems for investigation and settlement .........-.......--.. 320
Thea! PrODlRWNS . 65 sncwes oes k dots shes band ve cnt ote bb aes aoe eae 380. 3
Mepfioand land . [2-<:. pease cbaes eetecatat aye sees obumdk, 1s = ae 380
Wale Rdetis.. =: Xe Das dyschans dg becaeae ek ee es ae a oe eee 380
Maw. Branswiek.. 3. 5.6 Fcpvsins de o= Seles orvoates 4500 eens aa oe eee 381 a
Maite and New Hampshire<:. 2... 200.0 scc..cese X enone dapceenbeeus ~aer ES
Bastorn Massachwsetie’ ix sc. she eecdsc ous fseedwawee saat ee eT, ess
Maw Wott oc. sctaihtre ciwnn doe eke cet ke leaiua cen ene eee _. jae ee
Adirondack ‘sub-Province. ..> «224s = ben cuw'n bc eb Goeaw eee Ser
Wortiont.. sce. 2 obo dee des Sike toeee bebe ena dee eae 381 ‘ee
Canadian extension’: 2. ciciv c2s ee nts dhaet desc ote ad 330° =
Wow Jens69- 3562.42 Cyn eer oo coal tn ee ee eee cs Roe x: et
Pennsylvania .122...- (occic seb cage nati cceue gehen oS Sees
Grainy. c.06. 6... UVa ble ieco settee eee o jcei't 2. 383 S
N@rth Caroling 22. =5..~5- as <cayceu-ne sub ou des oes Page pa Seis Sea
MOnNOsSee .... 02-2 -loeee ca = cnaniccus sews hmuc'eusotbb ce cee fee
Georgia and Alabama 5... 2c s.cs2sn cede ok ods cake ee Rie Se
iitah ond Nevadawsis so 2 eed peoeecn eet bate en, eee 8 SE nck 384 a
Pimakeda! 55a, os es. eet Se 2 eer
Rocky Mountains ........ 00. oo ee Eee eget
MINS ok Xora S Sab Ue oe eke denle te tac Cae ok ee ee Ber eae .
Upper Mississippi Valley .-<---s<cec. cous soolse ccs. se ee
ME MSIIER ono wht WG on onc oaeek Gaaees be . ;
Problems affecting our knowledge of the Cambrian group as a whole or in ¢
DRAGS GROG 6 ois e's wintins visa Rats np dca aapein’d gh tned oe ma een a wim
Problems of nomenclature and classification...............--...---- BB. 3
INE STI D ogo 5 iS OE oe ok es ee tae) eee ag
The limit of the group. .... Se ce My Ona ree eg OTS ‘ae
+ 2 ee

Pe aN AR ie A a al es et Sede Wa!
Sr Ee ke os De ok A ; x y FER: y
eg i ie > ‘Se vs a A 4 ~ = ~
ron eer ae et eo ee =
, CONTENTS. — 9
; 7 2 F
eth ; “! 1 Page.

EF VI.—The ceetpetie and principles used by authors in the correlation
: “ 1e various parts ompring ‘the group, with observations on some methods
mado: ee ene tates: wi aed = Se - Sone gatlen ss «as Sete keenest es 391.

: a ‘Historical os tee ee eae sec Bs TE lt Sie ED Ee gee wee 391
> + fg América Sata ee es EE Oa ra eric s dlietgi a oO ewe = oe ahidel hit Date Sp wala iaon 391
-———- Maclure ...-....---.---.------- Picante ALA RAN Ge Ree etn pL eeeh eee
NMI Seay 56S cd debs ona c'ss awe vine cacwes eincnscbeceetpe nce mece 392
aes re otek Soca s Soda wacn ance dept vacs-e dass ccec-) | SOU
i? Jamies -.2....--. ithe, ie ae oe vias ei eae elon Au aco t nea 396
ie RGR e) POR pets Us 2.5. e cceenn ey ay RED BRR RS 2 TON TE 397
La ENON So OE aici 5 sc oseo be ve deve~ ces Gaswaaineot ogee 398
me -« Eaton ...... DN ee Wh A a awane win aeie 2 the een as oe 5 fon ee
IN = agg 22) 2-0 - --o onn eda oo ve no one e eae cn a cowemse 7399
“3 SP Sa al ei ae Rei PRO 401
I REE tee oa Sus as oS edn a na badewedce loedes 403
ERE CC Se eo ee Rn eer oo mE i 403
et ee ere aaa Sa Sasa mmcel oa cose Sats aad dees svoee nae~ 405
aaa Gre co cin = ok oass aoet <deea- oese <4 hae aes 405
~via. Pees ae hoa te he teh YT astintiee ese a ap ak dations wo empl 405
Newfoundland .........-..-.-----.- BE sie ied = lights inns ope, Sra ace 406
- Dana ie a ann Dé ig Sonraia ns ea vlan weeds a Secuan «ase oe natoeia doe 407
_ Mississippi Walley 2 S.552---23- i ah i Siale) Sh a atmo aha wip ha an she awe als Se 408
BN res enn gamer hee sts. ins chaps (cn = say nos-nokwlc died Tease - 408
Winchell SOUR eo aes ae Soaks ck sdk ews Uo owe es cdusimmtdedsd 409
i= || PME et eee ae eos So Pa. den cae axe oo oy Satan’ oFevew _ 410
Rocky RENE te epee a Gunde Lowen a an cane se aw8h one sees one So5c ae > AE
ae i ON, EIS eee Tea eens Dien |
ET CeG ds cin ca Baty ds K@cece ct cewes ec de s+ cach veders vceaeuau 411
Fortieth Parallel aie Sepa Tite Se PR, WEE AA AES IT 412
_. Explorations and Surveys West of One Hundredth Meridian...-.. 412
Geological Surveys of the Territories .-.-....---..-.--.--...----- 412
U.S. Geological Survey......-.- EEO Rad < o's paw hoeen Uae aoe 413
Correlations with European formations .................-..---- eerie 414 |
De Verneuil.........-- a ipl Phgid olen wind EEO od Gok a dni oe! ete 414
i eee bode at ere boda Doe gun ewaee eeu eae pai |
SEMIS Bho oNen CA 8 Sree sau awnu cbs ane vee oot Janta ou ate eae 416
ER Si ctiaia Fan «dee 4 Wns "ip swakod si0- cava Wao es wee hoses 417
Nae Sa EEE: a aa a aie” Ame Ray oer 418
Agassiz...... Peregirweses xo news oes Ree Sag whet a tk ston oe 419
OM IN eos oa Uaw vasa a ho coka 1~feke og~8erelele cae anaene 420
_ Methods RU RNase See a eee 421
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LETTER OF TRANSMITTAL.

DEPARTMENT OF THE INTERIOR,
UNITED STATES GEOLOGICAL SURVEY,
Tee DIVISION OF GEOLOGIC CORRELATION,
= PS te ; Washington, D. C., April 1, 1891.
Sir: q have the honor to transmit herewith a memoir by Mr. C. D.
Waleott, on the Cambrian of North America, prepared for peblicaner
as a bulletin. —
‘The Division of Geologic Correlation was created for the purpose of
summarizing existing knowledge with reference to the geologic forma-
a tions of North America, and especially of the United States; of dis-
_ cussing the correlation of the formations found in different parts of the ©
_ country with one another, and with formations in other continents;
_and of discussing the principles of geologic correlation.in the light of
_ American phenomena. The formations of each geologic period were ~
q assigned to some student already well acquainted with them and it was
_ arranged that he should expand his knowledge by study of the litera-
q ture, and by field examination of classic localities, and embody his
Tesults in an essay. The general plan of the work has been set forth
on page 16 of the Ninth Annual Report of the Survey, and on pages
x 108. to 113 of the Tenth Annual Report, as well as in a letter of trans-
ae mittal to Bulletin No. 80 of the Survey.
_ The first of the series of essays resulting from this work, prepared
ys ror Henry 8. Williams, pertains to the formations of the Car-
~ boniferous - -and Devonian periods, and constitutes Bulletin No. 80.
4 ‘The present essay is the second of the series, and others will follow.
Mr. Walcott finds that the American Cambrian includes three faunas,
Er of which the first and third are of continental range, and that by the
f; Em id of these faunas the formations in the various geologic provinces
: y be classified into three divisions, an upper, a middle, and a lower.
> finds also that these divisions may be homotaxially, and perhaps |
eee compared with divisions of the European Cambrian.
_ Very Respentfally, your obedient servant,
G. K. GILBERT,
Geologist in Charge.

Pig) Sy
ame
Bre 5

Hon “3 w. Paweir:
et ar eeecter U. 8. Geological Buses
¥ ~ 13

QUTLINE OF THIS PAPER.

This wovks is a etanes by one who is working in the Cambrian field, of the work of
“his predecessors, and of the results they and he have thus far obtained as he interprets
them. It thus becomes historical and descriptive, andis a general statement of the
| ss ae upon which the correlations have been made in establishing the group.

a a Chapter I gives a statement of the principles upon which the delimitation of the |

a group is based, a few brief remarks upon the nomenclature of the formations, and a
4 nae of the books and articles consulted in the preparation of this paper.

Chapter rat gives a historical review of the geologic and paleontologie work that
Fhe been done in the four provinces in which the sediments of the Cambrian group
‘occur. These are the Atlantic Coast Province; the Appalachian Province, which is

= into the Northern Appalachian and Southern Appalachian areas; the Rocky
~ Mountain Province, and the Interior Contineutal Province. The latiat is divided

a * into the Upper Mississippi Area, the Eastern Border or Adirondack sub-Province, the —
_ Western Border or Rocky Mountain sub-Province, and the Southwestern sub-Prov-

BF s ince of Texas and Arizona. Within each of the provinces the historical data are re-

- viewed by the eed divisions of States and Territories, and in British North
_ America by provinces.

‘fhe historical review of the geologic work embraces all that has come within the

: Ese inise of the writer of the descriptive geology of the rocks now referred to the
- Cambrian group. The paleontologic review includes only the mention of the genera
; > ands species described by the various authors.
\ Chapter 11 is a record of the names that have been employed to designate various
\. formations. It is of an historical rather than a controversial character.
Chapter Iv gives a summary of the present knowledge of the formations in each of
» & “the four geologic provinces, in the same arrangement as that of the historical review
| {i inchapterul. The attempt is made to give a concise statement of the present knowl-
| bs edge of the formations referred to the Cambrian group within each province. The
* _ paleontologic references are to the larger subdivisions of the fauna without mention
1 if “of genera or species. These will be described in special monographs, now in the
y course of preparation. At the close of this summary there is a synopsis of the Cam-
_ brian group, in which it is stated that the group is established by (a) the presence
in the Rocky Mountain Province of 6,000 feet of limestone with an undetermined
mass of quartzite beneath; (b) in the Appalachian Province by over 12,000 feet of

SSiastaite, shales, slates, eat limestones; (c) a continental distribution; (d) a charac-
Dt _teris tic, highly differentiated fauna. A table of the classification of the formations is
By. al wrranged with the type formation of each subdivision at the head, while beneath
are the formations correlated with it.

- Amap showing the geographic distribution accompanies this chapter ; also one
” on which the sedimentation is illustrated by vertical columns of strata. A section
er across the continent, with the base of the Ordovician fauna as the upper limit and
_ the columns of strata arranged beneath it, reveals the presence of a great trough
; © a ong the line of the Appalachians from Alabama to Labrador, and a second trough
onthe western side of the continent west of the eastern Rocky Mountain ranges.
Be ie claimed that the great interior Continental Province was a land area during
15

Fn
Es.
we

&.
4)

- ‘ - f “FF hb OO eS pe el .. <>. .
bee ie oe . ; TASS PE ae BY 7 AG

ee . =? > a

ahs ~ =

1600 Oe OUT Le or ‘THIS PAPER.

‘Lower and Middle Cambrian time and that the Oathbri an Sea aid net onion 7 upon it
until the beginning of Upper Cambrian time. A map based (PI. 11) upon this. view
illustrates the supposed land area at the beginning of Cambrian time. ~
The base of the group is stated to be where the oldest known fauna that is refétsed = Se
to the Cambrian fauna occurs. The summit of the group is the transition from the —
Cambrian to the Ordovician fauna, orin the New York section between the Pots- es,
- dam sandstone and the superjacent Calciferous formation. The rocks or sediments
are described and the conclusion reached that there were geographic areas in which | E
different types of sedimentation prevailed, and that as a whole the sediments were ‘
deposited in both shallow and deep waters on an ocean bottom that was being sowie
depressed in relation to sea level. %,
The study of the fauna indicates that the group may be conveniently divided into.
three divisions, lower, middle, and upper. The evidence of the sedimentation and —
organic remains proves the presence of geographic provinces in Lower Cambrian time —
that became more strongly differentiated in Middle Cambrian time and less strongly
marked in Upper Cambrian time. Sr
The chapter concludes by notes on the Cambrian rocks of Great Britain, Europe,
China, India, Australia, and South America. =
Chapter v deals with problems for investigation and sottioimant which are taken —
up, for the local problems, in the same order of presentation as thé matter in oa =
terst1andi1v. The general problems respecting our knowledge of the Cambrian —

. 7 4 4
jie ess ¥ een

-. group, as a whole, or in large parts, are discussed separately, as are the problems of

nomenclature and classification. The latter includes a statement of the problems —
relating to thename and the limits of the group.
Chapter VI is devoted to the study of criteria and principles used by authors in the
correlation of the various parts composing the Cambrian group, with observations —
on some methods of correlation. The first portion includes the historical notes, ‘ald ze
is a review in chronologic order of the principles of correlation used by authors in the 5
United States and Canada, and observations by authors upon correlation of American is
with European formations. This review shows that many authors have expressed _
sound views upon methods of correlation and that, with the exception of the addi- -
tions made since the theory of evolution began to influence paleontologists, ‘the |
addition to methods has been relatively small. Under the heading of methods of —
correlation, correlation by: superposition, organic remains, lithologic characters, é
and unconformity are treated of at some length. Under organic remains are con-— ss
sidered life zones, stage of evolution, life history, contemporaneity, homotaxis, and
percentage of species. Reference isalso made to homogeny and topographic features
as elements entering into the problems of correlation. : ; oa

x

THE OAMBRIAN GROUP OF ROCKS IN NORTH AMERICA.

- an ~
ae

ae By CHARLES D, WALCOTT,

CHAPTERI.

3 Sh INTRODUCTORY.

me This report is an unfinished memoir. It is an account of the present
knowledge of a great geologic group that will require prolonged inves-
Piccien to bring it to the status in descriptive geology already attained
cS. eu the superjacent members of the Paleozoic system.!
_ The uistory of the origin and application of the term Cambrian i in
: Ego eologic nomenclature is presented in connection with the description
_ of the names that have been employed in the classification of the various
Se rislisisdharacterized by the types of the ‘‘First or Primordial Fauna”
% of " Barrande. The basal fauna, as now known, is that of the Olenellus
_ tone ; and the upper horizon of the group is drawn at the summit of

The delimitation of the group is based on the principles: (a) that the
- great geologic groups must rest on the broad zoologic characters of
* ett included faunas, and not upon local stratigraphic breaks between
ertain series of rocks or upon local differences in sedimentation; (bd)
hat the most reliable chronologic scale in geology is that afford by
the e relative magnitude of zoologic change; and (c) that the geologic
ration and importance of any system are in strict proportion to the
F. Te iapacative magnitude and distinctness of its collective fauna. ?

Geologic classification has been largely based upon the imperfections
p the geologic record and an arbitrary assumption of breaks in the

¢ ain of sedimentation and life that are ndt of universal extent. Geo-

gic continuity must have been a fact and the sequence of life and
a depo osition continued uninterrupted on some portion of the earth from

earliest Cambrian time to the present day. Such continuity could

os

“not have existed in any one province, and it is doubtful if the complete

: sid cord. will ever be regained. In its absence the classification already

al

In the preparation of the historical portion I received material assistance from Prof. Joseph F.

abstracts which guided me in my historical research.

il. 812 rs) 17

the: series characterized by the Dikellocephalus fauna of North America.

tee

nei who, taking as a basis the bibliographic card-catalogue of Mr. N. H. Darton, prepared a series

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ERE ANE COMER TAM: ee eae

‘Satebhihed is adopted and then arbitrarily ‘ieee vyhaaee the oni = A
inal basis for it is cleared away by more perfect knowledge. — ae a
For convenience of description and geologic cartography, the geologic “a
formation! is taken as the primary unit of classification. The com-
bination of these primary units forms the terrane, which may be com-
posed of any number of geologic units. The groupings of the terranes
form the groups, and the union of the groups the systems. Thus the
Potsdam sandstone of the Adirondacks, the Dutchess County limestone _
of New York, the upper Knox shales of Tennessee, the Hamburg chai |
of Nevada, aad many other formations unite to form the Upper Cam-
brian terrane. The union of the Upper Cambrian with the Middle and
the Lower Cambrian builds up the Cambrian group. The combination — 4
of the Cambrian, Silurian, Devonian, and Carboniferous, forms the 4
Paleozoic system. “4
The nomenclature of the formations of any group frojuetitly ex- 3
presses in local terminology the history of the development or evolu. q
‘tion of knowledge of the group. For instance, the formations compos
ing the Cambrian begin, in America, with the “ Granular Quartz” and
then follow the Potsdam sandstone, the St. John shales, the Chilhowee
sandstone, etc. The plan of naming the formations from the locality —
at which they are best developed is a great safeguard and can be fre- 4
quently adopted. Forinstance, the Potsdam sandstone of New” York —
has its type locality at Potsdam in St. Lawrence County, where it can
be readily identified. Fotgdam in Bi Farmnance County, Cambrian —
or St. Croix sandstone of the Mississippi Valley, with which it has been
| identified, and to speak of the latter as the Potsdam sandstone, is to
Pe esti state that they are synchronous. The use of the name St. a”
Croix does not imply this. It enables the geologist to mention the
formation without assuming a correlation that he may or mer not be-
lieve in.

ey

1Dr. J. J. Bigsby states that ‘‘According to Deshayes ‘a formation is a space of time represen
a certain number of beds, laid down under the influence of the same phenomena,’ or, in other words, : a ¥
formation is characterized by the constancy of its fossils.” (On the Paleozoic basin of the State of =
New York. Part II. Classification of the Paleozoic strata of the State of New York. Quast. Jour. 3
Geol. Soe. London, 1858, vol. 14, pp. 428, 430.)

Adams ©. B. ), 1845, 1846, 1847, 1848.
gassiz (Alexander), 1863, —~
pashis (Louis), 1862.

_ Ami (H.) and Sowter (T. W. E.), 1887.

" _ Aveline (W.T.); Salter (J.W.), and, 1853.
: Bailey (L. W.), 1865, 1879.

Bi ailey ai W.) and "side aad (G. F.),

187,

¥ Bailey (L. W.); Matthew (G. F.), and,
=. 1869. -

Bailey (L. W.), Matthew (G. F.), and
Ells (R. W.), 1880.
— aily (W. H.), 1865.

i akewell (Robert), 1829. .

- rande (J.), 1846, 1852, 1853, 1860, 1861.
—=&B jarrande (Joachim), and Marcou (Jules),
1860.

Bayfield (H. W.), 1829, 1845.

E ebecher (C. E.) and Hall (C. E.), 1886.
“Be ell (Robert), 1879.

aie (Jules), 1888.

gsby (John J.), 1824, 1825, 1827, 1853,
< 1858, 1863.

Billing Ss (E.), 1860, 1861, 1862, 1865, 1872.
Br oS Semmatae ), 1860, 1872, 1873, 1874,

Br adhead | (G. C.), 1874, 1877, 1882, 1889.
ger (W. C.), 1886.

oks (T. B.), and Pumpelly (R.), 1872.
kley (S. B.), 1874, 1876.

. (William A.), 1849.

vin (S.), 1888.

\pbell (H. D. 4 1885.

ipbelll (J.), 1863.

spbell (J. L.), 1879, 1880, 1884.
apbell (J. L. and H. D.), 1884, 1885.
Campbell @. L.) and Ruffner (W. H.),

.
er

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Mme a OEE Lies
pares eae te : = = S é . ~
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pag eee - ke y > ~
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eo
‘LITERATURE.

_ LIST OF AUTHORS AND YEAR OF PUBLICATION,

Clemson (Thomas G.), 1835.
Comstock (‘I’. B.’, 1874, 1890.
Conrad (T. A.), 1839, 1840, 1841, 1842.

| Cook (George H.), 1863, 1868, 1874, 1884,

1885.

Crosby (W. O.), 1876, 1880, 1881, 1889.

Dames (Wilhelm), 1883.

Dana (Edw. §S.) and Grinnell (Ge B.),
1876,

Dana (James D.), 1863, 1872, 1874, 1877,
1885, 1887, 1890.

Dana (J. F. and S. L.), 1818.

' Daniels (Edward), 1859.

Dawson (George M.), 1384, 1886, 1887.
Dawson (J. W.), 1850, 1855, 1860, 1862,

1867, 1868, 1873, 1878, 1883, 1888.
D’Invilliers (E. ), 1883.

De la Beche (Henry), 1832.

Desor (E.), 1851.

Devine (T.), 1863. .

Dewey (Chester), 1319, 1820, 1824.

Dodge (W. W.), 1875.

Dutton (Clarence E.), 1881.

Dwight (William B.), 1886, 1887, 1889.

Eaton (Amos), 1818, 1820, 1822, 1824, 1828,
1830, 1832, 1839.

Elliott (John B.), 1883.

Ells (R. W.), 1887, 1889.

Ells (R. W.); Bailey (L. W.), Matthew
(G. F.), and, 1880.

Emmons (Ebenezer), 1837, 1838, 1839,
1840, 1841, 1842, 1844, 1847, 1856.

Emmons (S. F.), 1886.

Emmons (S. F.); Hague (Arnold), and
1877.

Endlich (F. M.), 1878, 1879.

Engelmann (H.), 1857.

Etheridge (R., jr.), 1883, 1890.

Ferrier (W. F.), 1883.

Fitch (Asa), 1850,

Fletcher (Hugh), 1877, 1878.

Foerste (A. F.); Shaler (N. S.), and, 1888,

Foerste (Aug. F.), 1889,

Fontaine (William M.), 1875, 1883.

19

a

ah)

20 hae THE CAMBRIAN.

Ford (S. W.), 1871, 1872, 1873, 1875, 1876,

1877, 1878, 1880, 1881, 1884, 1886.

Foster (J. W.), 18 49. .

Foster (J. W.) and Whitney (J. D.),
1849, 1850, 1851. ~

Frazer (Persifor, jr.), 1878, 1879, 1880,
1882, 1833, 1886.

Geiger (H. R.) and Keith (Arthur), 1891.

Geikie (Archibald), 1882.

Gesner (Abraham), 1836, 1841, 1843, 1845,
1849.

Gilbert (G. K.), 1874, 1875, 1890.

Grinnell (G. B.); Dana (Ewd.S8.), and,
1876.

Green (Jacob), 1834.

Hague (Arnold) 1881, 1882.

Hague (Arnold) and Emmons (S. F.), 1877.

Hall (Charles E.), 1881, 1885. (See
Beecher, C. E.)

Hall (James) 1839, 1843, 1844, 1845, 1847,
1851, 1858, 1859, 1860, 1861, 1862, 1863,
1873, 1884, 1886.

Hall (James) and Whitfield (R. P.), 1873,
1877. .

Hall (James); Logan (W. E.), and, 1866.

' Hartt (C. Fred.), 1865, 1868.

Harvey (M.); Hatton (Joseph), and, 1883.

Hatton (Joseph) and Harvey (M.), 1883.

Hayden (F. V.), 1858, 1859, 1861, 1862,
1863, 1869, 1871, 1873, 1874, 1875, 1885,
1888,

Henderson (J. T.), 1885.

_ Hicks (Henry), 1875.

Hind (H. Y.), 1869, 1870

- Hitchcock (C. H.), 1861, 1862, 1867, 1870,
1873, 1874, 1875, 1877, 1879, 1884, 1885,

, 1888, 1890.

Hitchcock (Edw.), 1832, 1841, 1859.

Hough (Franklin B.), 1847, 1850, 1851.

Houghton (Douglass), 1839, 1840, 1841.

Howell (Edwin E.), 1875.

Hubbard (Bela), 1849.

Hunt (T.S.), 1852, 1854, 1861, 1868, 1870,
1871, 1875, 1876, 1878, 1879, 1883, 1886.

Hyatt (Alpheus), 1885.

Irving (Roland D.), 1872, 1874, 1875, 1877,
1880, 1883, 1885, 1888.

Irving (R. D.) and Chamberlin (T.C.),
1885.

Jackson (C. T.), 1844, 1849, 1851, 1856,
1859, 1861.

James (Edwin), 1821, 1822.

‘Jenney (W. P.), 1874.

Johnston (J. F. W.), 1850.

Juxes (J. Beete), 1843, 1862.

apear (Benpanelie 1876.

King (William), 1&89.

| Meek (F. B.), 1868, 1870, 1871, 1872, 1573,

~

Kerr (W. C.), 1869, 1875. - =

Killebrew (J.B.), 1874
King (Clarence), 1876,1878. -
King (H.), 1851. es

Kloos (J. H.), 1882. Ae
Lane (Alfred C.), 1889. Saigey
Lapham (I. A.), 1851, 1855, 1869. *
Lapworth (Charles), 1881. Et,
Lea (Isaac), 1858. = ae
Lesley (J. P.), 1853, 1873, 1883, 1886 Cee
Lewis (H. Carvill), 1883, — as eee
Little (George), 1876. eas ot
Lloyd (T.G. B.), 1876. - a
Logan (W. E.), 1845, 1847, 1849, 1850, 1851,
1852, 1854, 1855, 1860, 1861, 1863, 1965, a
1866.
Logan (W. E.) and Hall (James), 1866, <i
Low (A. P.), 1884, 1886. A
Lydekker (R.); Nicholson (H. A.), and
1889.
Lyell (Charles), 1845.
Lyman (B.S8.), 1867. G
McConnell (R. G.), 1887, 1889. a
McCreath (Andrew), 1884. - “Gt
McCutchen (A. R.), 1884. az
McGee (W J), 1890. - a
Macfarlane (Thomas), 1867. _ ‘s a

if

Z, ae i, bets A Las
. Png ae y i pee
* ae + _—.

Maclure (William), 1809, 1817. ex ‘
Marcou (Jules), 1850, 1861, 1862, 1880, 1885,
1888, soe

Marcou (Jules); Barrande (J onctes and, —
1360. aitece
Marr (J. E.), 1880, 1883. ieee
Marsh (0. C.), 1869.
Marvine (A. R.), 1875. - ora.
Mather (William W.), 1841,1843.
Matthew (G. F.), 1863, 1865, 1878, 1883, —
1884, 1885, 1886, 1887, 1888, 1889, 1890,
1891.
Matthew (G. F.) and Bailey (L. W. ),1869, 3
Matthew (G. F.); Bailey (L. W.), and,
1872. iP
Matthew (G. F), and Ells (R. W.) ; eg
(L. W.), and, 1880. ga
Meads (A. D.), 1889. as ty

1877.
Meek (F.B.) and Hayden (F. V. ), 1858,
1859, 1861, 1864. 4
Milne (John) and Murrey. (Alexander),
1877. ‘
Murchison (R. I); Sedgwick cAdam),
and, 1835.

., 2 ~ wade

ene
<
oa

ae 1852, ie 1266, 1868,
1871, 1873, 1881,
heed 1), 1991. =

wood (J.C. ) 1852.
rdway (Albert), 1861.
“Rees 1843, eh 1851, 1852.

John P. 7 1867, 1868,

we 1 (S. W.), 1875,1876.

f me (Frederick, j jr. )s 1878, 1883.
out. (H. A. "f —

(T. D»,. 1889,

1 ardson (James), 1870.

athofen (F. F. von), 1882.

(S. ames), 1850.

ner (Ferdinand), 1849, 1852.

ers (Henry D.), 1838, 1839, 1840, 1841,

, 1846, 1857, 1858.

rs (Henry ‘D. and W. B. yy 1842.

vers rs (William B.), 1838, 1839, 1844,
6, 1861, 1875, 1879, 1884.

: nger (C.), 1873, 1887.

r r( W. H. ys Campbell (J. L.), and

n i AOvedke), 1879, 1883.
(J. M.), 1856, 1869, 1879.
(J. W.), 1859.

eraft (H. R.), 1855.
hn H.), 1390.
pte), 1838, 1852, 187 3.

y ca. C.), es 1879, 1883.
(N. S.), 1869, 1888, 1889,

(J. W.) and Aveline (W.T. ), 1853. |

Nero Sh wer ee fee hee Oe NS OR ee OP ee a ~

BS 7 of EE ie ee ae ;

alee ge Rae ‘a <
= ; 2
igs aes ay: LITERATURE, 21

‘Smith (E. A.), 1875, 1876, 1878, 1883, 1884.

| Smock (John C.), 1886.

Sowter (T. W. E.); Ami (H.), and, 1887,

Steele (John H.), 1823, 1825.

Stevenson (John J.), 1887.

Strong (Moses), 1877, 1880, 1882.

Swaliow (G. C.), 1855, 1871.

Sweet (E. T.), 1876, 1880.

Thompson (Zadock), 1853.

Todd (James E.), 1882.

Troost (Gerard), 1838, 1840, 1841.

Tuomey (M.), 1858.

Tyson (Philip T.), 1860.

Upham (Warren), 1884, 1885, 1888. .

Vanuxem (Lardner), 1840, 1842.

Verneuil (Ed. de), 1847.

Wadsworth (M. E.), 1880, 1882, 1884.

Wadsworth (M. E.); Whitney (J. D.),
and, 1884,

Walcott (Charles D.), 1879, 1880, 1883,
1884, 1885, 1886, 1887, 1888, 1889, 1890.
Webster (J. W.), 1824. ny
White (C. A.), 1870, 1874, 1875, 1876, —

1880.
White (George), 1849.
Whiteaves (J. F.), 1878.

Whitfield (R. P.), 1876, 1877, 1878, 1880,

1882, 1884,

Whitfield (R. P.); Hall (James), and,
1873, 1877.

Whitney (J. D.), 1855, 1858, 1862,1872, 1883.

Whitney (J.D.) and Wadsworth (M. E.),
1884.

Whitney (J. D.); Foster (J. W.), and,
1849, 1850, 1851.

Whittlesey (Charles), 1851, 1863.

Williams (H.S.), 1883.

Winchell (Alexander), 1861, 1864.

Winchell (N. H.), 1873, 1874, 1876, 1873,
1880, 1882, 1883, 1884, 1885, 1886, 1888,
1889.

Winchell (N. H., and H. V.), 1890.

Winwood (H. H.), 1885.

Wolff (J. E.), 1891.

Woodward (Henry), 1884.
Woodward (J.), 1723.

Wooster (L.C.), 1878, 1882, 1884.
Young (A. A.), 1882,

LIST OF PAPERS BY DATES.

1723.

-Woopwarp, Dr. J. An essay toward a Natural History of the Earth a and Terrestrial _
Bodies. London, 3d edition, 1723.

1809, vires

MACLURE, WILLIAM. Observations on the Geology of the United States Explanaiotee
of a Geological Map. Am. Phil. Soc. Trans., vol. 6, 1809, pp. 411-428, map.

= ie iN Aas
s

“\

1817.

MActure, WILLIAM. Observations on the Geology of the United States; with re- oJ
~ marks on the probable effects that may be produced by the decomposition ob
the different classes of rocks on the nature and fertility of soils. Witha map

and two plates. Am. Phil. Soc. Trans., new series, vob 1, 1817, PP. 1-91.

1818, : . q
Dana, J. F., and S.L. Dana. Outlines of the Mineralogy and Geology of Babine
and its vicinity, with a geological map. Am. Acad. Arts and Sciences, Me- :
moirs, vol. 4, 1818, pp. 129-223.
EATON, ‘Amos. An Index to the Geology of the Northern States, with a transverse lq
section from Catskill Mountain to the Atlantic. Leicester, 1818, pp.52.
R(AFINESQUE) C.S. Observations on the Geology of the United States of America, 4
by William Maclure; a notice. Am. ere Magazine, vol. 3, 1818, pp.
41-44,

1819. , PaaS

Dewey, CuEsTER. Sketch of the Mineralogy and Geology of the Vicinity of wil-
liams’ College, Williamstown, Mass. (With a map.) Am. Jour. apo vol. te
1819, pp. 337-346. .

1820. Kee ae

DEWEY, CHESTER. Gsalsaeat section from Taconick Range, in Williamstown, to ‘

"the city of Troy, on the Hudson. Am. Jour. Sci., vol. 2, 1820, pp. 246-248.
Eaton, Amos. An Index to the Geology of the Northern States. "2d Ed., Troy,
; N. Y., 1820, pp. 286.

1821. Sees < 4

JAMES, EDWIN. Remarks on the sandstone and floetz formations of the western part 4
of the valley of the Mississippi. Am. Phil. Soc. Trans., new series, vol. i
1821, pp. 191-215.

1822, 4 a

‘Earoy, Amos. A geological and agricultural otter of Rensselaer County, N ew York, ee
with a geological profile, from Onondaga to Massachusetts. Albany, 1822,
pp. 70, plate. Memoirs of the Board of Agriculture of the State of New ;
York, 1823, vol. 2, pp. 3-43. .

JAMES, EpwIn. Geological sketches of the Mississippi Valley. Phila. Acad. Seis 4
Jour., vol. 2, 1822, pp. 326-329.

SLES So ae CTE et a SOU OS Ror a e Sealaae e See n J . =
= 3 ae > > c “es -f 5; & ,
= a. Rd a tee ‘ «—

1, JOHN | H. toport of ‘the eooliibaodT structure of the county of Saratoga.
Ptiantice of the Board of Agriculture of the State of New York, vol. 2, 1823,
- ~pp. aoe, 155-161.

ge 5m 1824.

rE

iB BiasBy, . JOHN J. A list of mineral and organic remains occurring in the Canadas.
Am, Jour. Sci., vol. 8, 1824, pp. 60-88.

| SEER. CHESTER. A sketch of the geology and mineralogy of the western part of

cy : _ Massachusetts, and a small part “of the adjoining States. Am. Jour. Sci.,

+. -vol. 8, 1824, pp. 1-60.

‘Earow, Amos. A geological and agricultural survey of the district adjoining the

Erie Canal. Albany, 1824, pp. 163, plate.

W WEBSTER, J. W. Remarks on the geology of Boston and its vicinity. Boston J our.

Phil. and Arts, vol. 2, 1824, pp. 277-292.

~ aes
Ne bps °
nl Se 1825.
ee. me ‘ ,
%

q Brospy, J.J. Notes on aie geography ash geology of Lake Superior. Quar. Jour.
_- Lit., Sei. and Arts (of the Royal Inst. of Gt. Britain,) vol. 18, 1825, pp. 1-34,

ey t;, 228-269, map.

a ig - county of Saratoga, and State of New York. An. Jour. Sci., vol. 9, 1825, pp.

gia 16-19.

ee Si 1827.

“Brospy,

J.J. On the geology of Quebec and its vicinity, Geol. Soc. Lindéu Proce. ay
vol. 1. 1827, pp. 37, 38.

1828,

Ey ‘TON, Amos. Geological nomenclature, exhibited in a synopsis of North American
g i: : _Tocks and detritus. Am. Jour. Sci., vol. 14, 1828, oppo. p. 144, pp. 145-159;
M 359-368.

= . Annunciation of the second part of Prof. A. Eaton’s report of the geological
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=: 1829.

AK :WELL, omane, tuteotiackion to Geology, ‘Ist American Edition, New Haven,
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1830.

Piiscos. - Geological text-book, va een for popular lectures on North Ameri-
ean geology; with applications to mer igniear’ and the arts. Albany, 1830,
aa pp. 64, pls. and map.

>
a ¢ «re 1832.

A BrcuE, aden: Geological Manual, Philadelphia, 1832.

N, AMos. Geological text-book for aiding the study of North American Geol-
ee) SOry 5 being a systematic arrangement of facts collected by the author and
_.* his pupils under the patronage of the Hon. Stephen Van Rensselaer. Second
. edition. 5 plates. Albany, 1832.

— Geological equivatents. Am. Jour. Sci., vol. 21, 1832, pp. 132-138.

—— Four cardinal points in stratigraphical geology established by organic remains.
Am. Jour. Sci., vol. 21, 1832, pp. 199-200.

cock, Epw. Report on the geology of Massachusetts; examined under the
direction. of the government of that State during the years 1830 and 1831.
Am. Jour. rad vol. 22, ae pp. 1-70, with map.

oe 8 ORS

cage” SIAVERATURE, ee 8 te ker
1 ae Sea ; Far a : ; Z
ety ORS.

Le, 3 JounH. A description of the Oolitic Formation lately discovered in the

=

2. Seopa THE CAMBRIAN, vt
mS 1834, — an Seas ee
GREEN, Jacos. Descriptions of some new North 5 ictatan trilobites. Am. Jour. §
- vol, 25, 1834, pp. 334-337. oss
1835. reed é

CLEMSON, Tuomas G. Notice of a geological examination of the country between wa

; Fredericksburg and Winchester, in Virginia, including the gold region. oe
Geol. Soc. Pennsylvania, Trans,, vol. 1, 1835, pp. 298-313. (Colored map of ee
sections. ea
SEDGWICK, gels and R. I. Murcuison. On the Silurian and Cambrian systems, ~
exhibiting the order in which the older sedimentary strata succeed ea “6

other in England and Wales. Brit. Assoc. Report for 1835, part 2, pp. SeGhe

1836. | oS

“ganna? ABRAHAM. Remarks on the geology and mineralogy of Nova Scotia. Halie
fax, N. S., 1836, pp. 272. ,

- 1837. ad ie ae

_ Emmons, EBENEZER. First annual report of the toil geological district of Waiwe. :
York. First annual report of the geological survey of New York, ba
1837, pp. 97-150; map. . . s

1838.

ait Ones EBENEZER. Report of the geologist of the second geological district of N: ewe
York. Second annual report of the geological survey of New York, Albany, —
1838, pp. 185-250; pl. 4, map. ;
ROGERS, Henry D. Second annual report on the geological exploration of the State -
of Pennsylvania. Uarrisburg, 1838, pp. 93, plate. a
Rogers, WILLIAM B. Second report of the progress of the geological survey of the
State of Virginia, for the year 1837. Richmond, 1838, pp. 24. (This report
occupies pp. "147-188 in the reprint ‘‘ Geology of the Virginias,” New York, | i
1884. ) :

~~"

SEDGWICK, ADAM. A synopsis of the English series of stratified rocks inferior to +he. 34
old red Sandstone, with an attempt to determine the successive natural — 4
groups and formations. Geol. Soc. London, Proc. vol. 2, 1838, pp 75-685
(read May 23, 1838).

TROOST, GERARD. Fourth report of the geologist of the State of Tennessee. — Nash- :
ville, 1838. Map, pp. 628-652.

”

; 1839, | 3 a

ConraD, T.A. Noteson American Geology. Am. Jour. Sci., cat 35, 1839, pp. 937-251, Neo

Second annual report on the paleontological department of the survey. Thir ~

annual report of the geolo icalsurvey of New York, Albany, 1839, pp. 57 ae

Eaton, Amos. Cherty Limerock, or Corniferous Limerock, proposed as- ‘the line of n
reference for State geologists of New York and Pennsylvania. Am. Jour.
Sci., vol. 36, 1839, pp. 61-71, 198.

EMMONS, EBENEZER. Third annual report of the second geological. diniriets Third - +9
annual report of the geological survey of New York, Albany, 1839, pp. 201-230.

Harty, James. Third annual reportof the fourth geological district of New York.
Third annual report of the geological survey of New York, Albany, 1839, <4

pp. 287-339. --

Hoventon, Doverass. [Peninsula District.] Second annual report State seiloeiatg
of Michigan, Detroit, 1839, pp. 4-39.

Rogers, Henry D. Third annual report on the geological survey of the State of
‘Pennsylvania. Harrisburg, 1839, pp. 119.

RoGERS, WILLIAM B. Report of the progress of the geological survey of Virginia, —
for 1838 (Richmond, 1839), pp. 32. (This report occupies pp. 189-244 of esis
reprint ‘Geology of the Virginias,” New York, 1884.)

Sooke oc eeaactirmas ares ri 25
= eee eee a one y

eee Somes |" ae ; Bi

Tr. Le On the Silurian yeteias with a table of the strata and characteristic
‘ 3. Am. Jour. Sci.,-vol. 38, 1840, pp. 86-93.
| EBENEZER. Fourth annual "report of the survey of the second geological
ee Rais et of New York. Fourth annualreport ofthe geological survey of New
ao omer 1840, pp. 259-353.
( yN, DOUGLASS. Third Ann. Rep. State Geol. of Michigan. House Reps.
a _ Document No.8. 1840, pp. 33.
+ERS, HENRY D. Description of the geology of the State of New Jersey, being a
iS final report. Philadelphia, 1840, with plate and map. pp. 301. .
_ — ‘Fourth annual report on the geological survey of the State of Pennsylvania.
Harrisburg, 1+40, pp. 252.
=~ 908 ST, GERARD. Fifth geological report on the State of Tennessee. Nashville,

1840, pp. 44, 3 maps.

Eee Fourth annual report of the geological survey of the third
district. rth report of the geological survey of New York, Albany, 1840,

1841.

RAD, T. A. Fifth aontvant report on the paleontology of New York. Fifth annual
- report of the geological survey of New York, Albany, 1841, pp. 25-57.

v 10NS, EBENEZER. Geology of the Montmorenci. American Magazine, vol. 1, 1841,
pp. 146-150.

NER, ABRAHAM. Third report on the geological survey of the Province of New
oie ‘Brunswick. St. John, 1841, pp. 8

'CHCOCK, EpwarRbD. Final report on the pe of Massachusetts, 2 vols., Amherst,

. Be: e. 1841, vol. 1, pp. x11, 299; vol. 2, pp. 300-831; 55 pls.

eee Doverass. Report [on the Northern or Upper Peninsula]. Geol. Survey
_ Michi an, 4th Ann. Rep. State geologist, 1841, pp. 4-89.

W.W. - Fifth annual report on the geological survey of the first geological
aay Fifth annual report of the geological survey of New York, Aibany,
1841, pp. 63-112.

RS, H. D. Some observations on the geological structure of Berkshire, Massa-
- chusetts, and neighboring parts of New York. Am. Phil. Soc., Proc., vol. 2,
1841, pp.-3, 4,

- _ Fifth annual report on the geological exploration of Pennsylvania. Harris-
: = ane burg, 1841, pp. 156 and plate.

ROO ST, GERARD. Sixth annual report of the geological survey of Tennessee by the
‘s State geologist. Nashville, 1841, pp. 48. :

‘THER

-

3 oe - 1842,

NRAD T. ay Observations on the Silurian and Devonian systems of the United
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=i oa 1842, pp. 228-235.

Emi ENEZER. Geology of New York, part 2, comprising the survey of the
Fa a ‘second geological (northern) district, 1842, pp. 438, pls. 17.

— Topography, geology, and mineral resources of the State of New York.
aa of the State of New York, by J. Disturnell, Albany, 1842, pp. 5-25.
, H. D,, and W. B. Rogers. On the physical structure of the Appalachian
Chain, as exemplifying the laws which have regulated the elevation of great
mountain chains generally. Brit. Assoc. Rept., Vol. 12, Trans. Sece., pp. 40-42;
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EM, _ , LARDNER. Geology of New York. Geology of the Third (central) Geo-
logical District. Albany, 1842, pp. 307.

oo ee >

1843.

ABRATIAY. Report on the Geological Survey of the Province of New Bruns-
vick, with a Topographical Account of the Public Lands and Districts Ex-
lored i in 1842. St. Jobn, 1843, pp. 88.
— Memoir of the Geology of Nova Scotia, with a map. Geol. Sce. London, Proc.,
e “Vol. 4, 1843, pp. 16-190.
4 JAMES, Geology of New York. Geology of the Fourth (western) Geological
istrict. _ Albany, 1843, pp. xxvii, 686, 19 pls. and map.

*
oo,

ad

Bete aCe nee THE CAMBRIAN. PRR : Bettie oe a
: > ; r i Eons ee % 4

~

Haut, James. Geological map of the Middle and Western States. Geol. of New
York. Rep, on the Fourth Geological District, Albany, 1843. < a
Notes Explanatory of a section from Cleveland, Ohio, to the Miscieipy Di z
~ River, in a Southwest Direetion; with remarks. upon "the Identity of th
Western Formations with those of New York. Assoc. Am. Geol. Trans., 1843,
267-293. .
JUKES, F'R. General report of the Geological Survey of Newfoundland in 1839 and :
1840, London, 1843, pp. 160, 2 pls.
- MATHER, WILLIAM W. Geology of New York; Geology of the First (southeastern)
District. Albany, 1843, pp. xxxvii, 655, 46 pls.
OweEN, Davip DALE. On the Geology of the Western States. Am. Jour. Sei., vol. |
45, 1843, pp. 151, 152, 163-165. al

'

(1844. toa
Emmons, E. The Taconic Syatem ; based on Observations in New York, Massachu- cS
setts, Vermont, and Rhode Island. Albany, 1844, pp. vii, 67, 6 pls. ‘
_ HALL, JAMES. Geological Survey of New York; its Influence on the Productive Pur- a
suits of the Community. New York State Agr. Soc. Trans. for 1843, paste pp.
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JACKSON, C. T. Final Report on the Geology and Mineralogy of the State of New |
Hampshire, with Contributions towards the Improvement of Agriculture and
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Rogers, HENRY D. On American Geology and Present Comlition of Geological Res
search in the United States. Am. Jour. Sci., vol. 47, 1844, pp. 137-161, 247-278.
Roaers, W. B. A System of Classification and Nomenclature of the Paleozoic Rocks |
of United States, with an Account of their Distribution more Particularly in
the Appalachian Meuntain Chain. Am. Jour. Sci., vol. 47, 1844, pp. 111, 112.

1845. ; pe ere

Apams, C. 2 First Annual Report on the Geology of Vermont. Burlington, 185
2. a
Beauseeo. H. W. On the Junction of the ‘Taneition and Primary Rocks of Canada
and Labrador. Quart. Jour. Geol. Soc., London, vol. 1, 1845, pp. 450-459.
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son and Richard Brown.) Quart. Jour. Geol. Soc., London, vol. 1, eyed }
oppo. p. 23. A
HALL, Samus. Nature of the Strata and Geographical Distribution of the Organic :
Remains in the Older Formations of the United States. Boston Jour. Nat. |
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LoGaN, W. E. (Account of General Structure of an Extended Area in- North
America.) Geol. Survey Canada, Report of Progress for 1843. 1845.
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pp. 231. Le
1846. : feat 4
Apams, C. B. Second Annual Report on the Geology of the State of Vermont. “Bore * re
lington, 1846, pp. 267. oe
BARRANDE, J. Notice Préliminaire sur le Systeme Silurien et les Trilobites de Bo-
héme, Leipsig, 1846.
RoGeErs, H. D. On the Mineralogy and Geology of the South Shore of Lake Super
‘jor. Boston Soe. Nat Hist., Proc., vol. 2, 1846, pp. 124, 125. .
. \
1847. 5
_ Apams, C. B. Third Annual Report on the Geology of the State of Vermont. Bur- 4
lington, 1847, pp. 32. (See foot-note on page 31). ‘4
On the Taconic System. Am. Jour. Agri. and Sci., vol. 6, 1847, p. 260 on
rected pagination).
_Emmons, E. [On the Taconic system.] Am. Jour. Agri. and Sci., vol. 6, 1847, Pe
260 (corrected pagination).
Agriculture of New York, vol. 1. Albany (1846), 1847, pp. 371, pls. 21, aad <
HALL, JAMES. Paleontology of New York, vol. 1, Containing ‘Descriptions of the Or- ©
ganic Remains of the Lower Division of the New York System. Albany, — j
1847, pp. xxiii, 338, pls.
- Letter on Certain Fossils in the Red Sandrock of Highgate. Third Annual
Report on the Geology of the State of Vermont. Ra SS 1847, eR 31. a

‘ . — *
° tees

?
>
~
3 .
¥
¥
Ve
1
~

7
\

Ho os iit: B. i Src er on as bisaiaey. of Lewis County, New York.
__. Am. Jour. Agri. and Sci., vol. 5, 1847, pp. 267-274, 314-327.’

Loc G: .N, W. E. Report on Sequence and Distribution of the Formations [on the Otta-
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~7

“VERNEUIL, Ep. DE. Note sur le parallelisme des roches des dépéts paléozoiques de

1 See VAmérique Septentrionale avec ceux de l’Europe, suivi d’un tableau des
_——snespécess fossiles communes aux deux continents, avec l’indication des étages

~~ ott elles se rencontrent, ef terminé par un examen critique de chacune de ces
ie ie oe _especes, Soe. véol. France, Bull., 2° sér,, vol. 4, 1847, pp. 646-709. Trans-
: lated with a.otations by Prof. James Hall, Am. Jour. Sci., 2d ser., vol. 5,
finns PP: 176-183, 359-370; vol. 7, 1849, pp. 45-51, 218-231.

Z oe eS oe 1848,

Roaws, ©.B. On ind Taconic Rocks. Am. Jour. Sci., 2d ser., vol. 5, 1848, pp.

ig 110.

We Owen, D.D. (Letter on Geology of Wisconsin Territory.) Soc. géol. France. Bull.

ie 2¢ sér., vol. 5, 1848, pp. 294-296.

a -_ Report of a Geological Reconnoissance of the Chippewa Land District of Wis- .

-—- gonsin; and Incidentally of a Part of Iowa and of the Minnesota Territory.
Rot Detter of the Secretary of the Treasury Communicating a Report of a Geo-

logical Reconnoissance of the Chippewa Land District of Wisconsin (etc), by

—————sS*&D. D. Owen, Thirtieth Congress, first session. Senate Ex. Doc. No. 57. 1848.

ase’: pp. 3-72, map, plates.

1849,

Bort, WILLIAM M. Siena y and Geology of the Survey, with reference to mines
“ +x. and minerals, of a District of Township Lines South of Lake Superior in 1845,
ae Message President United States, Thirty-first Congress, first session, H. R.
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Foster, J. W. Notes on the Geology aud Topography of Portions of the Country
Se Adjacent to Lakes Superior and Michigan, in the Chippewa Land District.

i a Yt “Message from President of United States to Congress, Thirty-first Congress,
aot first session, H. R. Ex. Doc. No.5, part 3, 1849, pp. 773-785.

Fo STER, J. W., and J. D. WHITNEY. Synopsis of the Explorations of the Geological
ag “Corps in the Lake Superior Land District in the Northern Peninsula of Michi-

2. Message from the President of United States to Congress, Thirty-

; a

Bark rst Congress, first session, H. R. Ex. Doc. No. 5, part 3, 13849, pp. 605-625,

cs _ 3:maps.

oa ape ABRAHAM. The Industrial Resources of Nova Scotia. Halifax, N. S., 1849,
. pp. 341, and Appendix, p. 15.

BARD, BELA. | General Observations upon the Geology and Topography of the

District South of Lake Superior, Subdivided in 1845, under Houghton. Mes-
_ ‘sage from President of United States, Thirty-first Congress, first session, H.

~~ R. Ex. Doe. No.5, part 3, 1849, pp. 833-842.

Jackson, C. T. Message of President of United States to Congress. Thirty-first
. _ Congress, first session, H. R. Ex. Doc. No. 5, part 3, 1849, pp. 371-502. |

_ Logan, W. E. Canadian: Geological Survey, Report Progress ‘for 1847-48, 1849.
Ror IMMER, FeRD. Texas. Mit besonderer Riichsicht auf deutsche Auswandcrung und
Beee ss die physischen Verhiltnisse des Landes nach eigener Beobachtung geschil-

dert. Bonn, 1849, pp. 464, map.

TE, gens Statistics of the State of Georgia. Savannah, 1849, pp. 624 and
7. map

1850. .

WSON,, J. Ww. ‘On: the Metamorphic and Metalliferous Rocks of Eastern Nova Sco-
tia. Quart. Jour. Geol. Soc., London, vol. 6, 1850, pp. 347-364.
PY CH, Asa, M. D. A Historical, Topographical, and Agricultaral Survey of the
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; ee 753-944,
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du lac Superieur. ] Soc. géol. France, Bull., 2° sér., vol. 8, 1850, pp. 89-100.
— — Report on the Geology and Topography of a Portion of the Lake Superior
53 Land District in the State of Michigan. PartI. Washington. 1850. Strati-
“ aa q - fied aad Sedimentary Rocks. Chapter A, pp. 99-122.
“Sal ew 4 ay se etre |

3 r J 3
a, ae va eX

ae fe Cen Meera et) Bere Ge

. 5 ; i) " «4 ne ae Err ix Sed ee
> , oo 2 Aen ? : “CK » « ) Tage a . a
28 THE CAMBRIAN. OES OS ies
: ; Ot TU Sareea

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ae umremaroRs. 29

~

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< Ie nosgt tee oi . ROE ee ee
S00. AS : THE CAMBRIAN. 2 fBULL SL

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\ f Rhone

i? 7 Romy ee Me es 7 FE, Mt hl Sa Vy eS tee ‘\ +. a i _ = s - - xpd
Same bee yee fay eit <a t . r “ . y A ie ox .
oP ay a re : “ nae ; =
BER _ LITERATURE. ” 31.
ep Me ~ ¥

cot ee rel Kaa

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~~ ~ : ~

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~- Me Ps Ad Lo ear CS i? Aw ‘3 a eo oe.”
r i eo Se ~ e a - & a 2 4 > ran eps Oe. ‘ ve Wet Fe’
: * > » an . IY a ak ae : ‘ rs cy al iy ro

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sh tee | LITERATURE. ¥ 33

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—

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36 : THE ‘CAMBRIAN. ‘ :

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CLE ET et ete ae ae ee ee
tee tee a fy ETERS BO ROPES I lm SI ae
ust ay st A Ee gre ea, ae ea

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1 ~ Es > , c
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we « ©" ees. ¥ ue ® ~y — ~~ > - . ~ ¥. 9 “es
; " ri he le = ar 21 oe i, = ~ J =. 4 ~

PPPs

~ =

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Pe \ Cc

+
a -

ne
ia

4
?

BELL, N. H. Notes on the age of the rocks of the Mesabi and Vermilion iron

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a DWARD, HENRY. Notes on the remains of Trilobites from South Australia.

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_ Sour. Sci. ., od ser., vol. 27, 1884, pp. 463-465.

as * oN! gis eee ‘ : rte De

: : Se ee Wie ae Pade MoE ‘x ae *
44 ie Oeety : “THE CAMBRIAN. ©. — (BuLL, a. ©
Ne ria (.”.): Relies ears fai. a es Saute a
‘ Camenzxt, H. D.. The Potsdam group east of the Blue Ridge at Balcony Falls, vas a

By ginia. Am. Jour. Sci., 3d ser., vol. 29, 1885, pp. 470-474.

~ CAMPBELL, J.L,and H. D. CAMPBELL. Review of: William B. Rogers’s Geology of |
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/

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<u

HAYDEN, F. V. (Report of the Moutana division.) U. 8. Geol. Survey, 6th Ann. -

Rep., 188485, 1885, pp. 48-53.

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E: “ \
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7 ;
i r >.

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x

«

ds ew ere

4

1s

<4

a
¢

a yaa aeoamn ce toed ‘ $e . ETON ‘ i yy a , j Z ; : o
aa oan Ge LITERATURE, | 45
‘Pe. was Sa PON . ‘
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4

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*

AGE ‘THE CAMBRIAN, pone
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a Ee

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1
4
7
4

$3

‘ 4

<4
.

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~~

1889.

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~ — ~

3
é : .«~ as a | wd

OE Ss. Sage ae ate - *
“.

regs _ LITERATURE. “iguey lowest oa

—

J
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ip a
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,
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a
~y
as:
a

>
mee! «2

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Rae

~~ *

+e 7 ; ee
ee

w'
eS ¢
ee lee
Re? & AS 4s
¢ © ee ahs o .
‘ ES e -- ? Re ae

tarry

~ Canada

aso, ras ae Ge le cg 1. ; 1891, eae
m. Geolo vol. 7, , pp:
n, N. 8., id I On the geology, of it Pl
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Pi

cain

i ~~ i
4
. wee d
arts “9 Bey 7 .

: CHAPTERIL.

UISTORICAL REVIEW OF THE GEOLOGIC AND PALEONTOLOGIC
WORK.

_ ‘The scope of this review is limited, with a few exceptions, to the no-
ice of papers and memoirs that have added something original to the
existent aru leige of the rocks and faunas now referred to the
- mbrian group.

everal methods of presenting the historical data have suggested
themselves. 5

4 ) Chronologic ; (2) Geographic and chronologic ; (3) psi ga
g graphic, and stratigraphic.

B41): Chronologic.—This method necessitates reference to papers in ae
ler of their. publication, whether they treat of Cambrian rocks in
Newfoundland, New York, Alabama, or Nevada. All is subservient to
th ¢ chronologic record. |

(2) Geographic and chronologic.—This method permits of the chrono. .
lo grouping of the papers referring to the rocks under consideration
in geographic areas.

(3) 3) } Chronologic, geographic, and stratigraphic.—This third and more
omprehensive method arranges the review in the form of a statement
Le historical data as in the second « sigue with the addition of

8 Lainct Cambrian ; second, Middle Cambrian; third, Upper
‘tian. This nomenclature will be used throughout the review,
tis necessary to refer to a standard generally known.

_of Cambrian age occur on the North American continent in
cipal geographic: areas or geologic provinces. In. reviewing

a

The . Se rastic Coast or Hastern Border Pebinen
he Appalachain Chain. 3
2 ae Che ¢ Rocky Mountain or Western Border Province.
t Bu ul soma 4 49

_ J. Beete Jukes, who in 1843 published a report of his studies in field —

~Soe., London, vol. 1, 1845, pp. 450-459.

ite Ceeigntts thet: vide 1S eras PARES INNS Baas AOL ae ee
tre : Sigick i, ; = Nie eigen eee aes Page —

es) cee ‘4 Ar ey 4 ge ae eae EE, eee

oe foes d ~ NS Se Pate.

; ‘rr , FON te ie SS eee

50 aa a THE CAMBRIAN. NUL ae ST ee

tion could be followed, though in an interrupted ling, from Brainwree,
_ to Newfoundland.' iy

IV. The Interior Continental or Central Proviiios.
The record of paleontologic investigation in each province will fot
low the geologic review.

ATLANTIO COAST PROVINCE,

The Atantic coast province includes the deposits on the island of
Newfoundland, the provinces of Nova Scotia and New Brunswick and
Cape Breton, and the States of Maine, New Hampshire, and eastern
Massachusetts. Sie | i ;
NEWFOUNDLAND.

Systematic geologic investigation in Newfoundland began with Prof. 4

and office. He describes the relation of the strata at the base of the —
Paleozoic section (now referred, to the Olenellus zone), to the uncon-
formably subjacent crystalline rocks about Conception Bay, and men-
tions the red shales in which the Olenellus fauna is now known to"
occur, as well as the green and dark shales of the Paradoxides zone, as _
subsequently known.. A description is given of the upper slate for: 4
mation as shown on the islands in the bay, under the name of Bell |
Island shale and grits; and of the lower slate under the name of St.
John’s slate, 2,000 to 3,000 feet thick, as seen near the town of St.
John’s ; also the superjacent Signal Hill sandstone, about 800 feet thick. 2
In the absence of fossils no attempt was made to correlate the forma-— q
tions with those of England. On the map accompanying the report .
the geographic distribution is given of the lower slate (St. John’s) and —
of the upper slate (Bell ee) formations about Conception Bay and
Smith Sound. ‘ é

Two years later Capt. H. W. Bayfield’ described a savdaiains with j
subjacent red and white limestone on the Straits of Belle Isle, which |
he stated contained a species of Cyathophyllum. This is the first notice —
of the Lower Cambrian rocks containing Archeocyathus, and it is thea
second recorded discovery of fossils now referred to the Olenellus zone. —

Ata meeting of the Boston Society of Natural History, April 20, 1859,
Dr. C. T. Jackson exhibited a trilobite from the calcareous slate of St. —
Mary’s Bay, Newfoundland, which he thought identical with Paradox. —
ides harlani from iat, Massachusetts. He said that this forma-— 4

In 1859 Mr. J. W. Salter ® received a specimen of the genus Paradox: | |

1 General report of the geological survey of Newfoundland in 1839 and 1840, pp. 160, pls, Tondon, z
1843. .
2Op. cit. pp. 55-60. - nie
3 On the junction of the transition and primary rocks of Canada and Labrador. Quart. #4 our. Geol.

40Qn a trilobite from Braintree. Boston Soc. Nat. Hist., Proc., vol. 7, 1859, p.54. ;
5 On the fossils of the isnanlasings or ‘‘Zone Primordialo.” Quart. Jour. Goel Soc., London, vol,
15, 1859, pp. 551-555. a, 4

l :
. a

wpe a
cy

ed ie.
ut ; Ay > ex ‘<p

Sa ee gad NEWFOUNDLAND. 51...

3 i “ides, ¢ Apissted from the upper slate of St. Mary’s Bay, Newfoundland, |
which he described under the name of Paradowides bennetti, calling
- ‘attention to its relation to Paradowides spinosus and P. bohemicus, of
| Bohemia.
e.- Iw 1862, Prof. Jukes, dieing to his work in Newfoundland, stated
“4 - that he included under the upper slate formation the Bell inte shale
and gritstone and variegated slate; and in the lower slate formation the_
_ Signal Hill sandstones and St. John’s slate. He says he did not find
| any fossils in them, but that Mr. C. Bennett subsequently found trilo-
_ bites of the genus Paradoxides (named P. bennetti by Mr. J. W. Salter)
> in the slates on the west side of St. Mary’s Bay. ‘+ These slates belong
4 “to the ‘group I called the St. John’s slate, which is covered conformably
4 a by the Signal Hill sandstone. The Variegated slate group, on the other
_ hand, passes up into the Bell Isle shale and gritstone, and near Brigus ©
~ Harbor, in Conception Bay, may be seen to rest unconformably on the
_ St. John’s slate” (as described in 1843).! This is the union See
now recognized between the Cambrian and Algonkian rocks.
oa ‘Highteen years after Captain Bayfield had reported on the strata of
the north side of the straits of Belle Isle, Sir William E. Logan? des-
5 - cribed the strata resting on the gneiss as red and green. sandstones, 231
feet thick, overlain by gray, reddish, and greenish limestone. In thelime-
Pk “stone a number of fossils were found which Mr. Billings identified with |
& found i in the “ Red-Sandrock ” of Vermont. The formation was re-
_ ferred to the Lower Potsdam by Logan. Fifteen miles across the straits,
“_on the Newfoundland coast, the rocks are apparently of Calciferous age;
ES c and he concluded that the Pandan sandstone zone was buried beneath
a ne waters of the Straits.’ In the description of the section at Bonne
Bay, on the west coast of Newfoundland,‘ it is compared with that at
‘ the Straits of Belle Isle; and on pages 865-867, the section at Bonne
= Bay is given in detail. Of this 1,711 feet are, by the contained fossils,
s referred to the Potsdam group.
. oy the report of the Geological Survey of Newfoundland for 1864° a
s s mary is given of the then existing view of thesuccession of the Lower
be aleozoic rocks in North America. For Newfoundland the succession —
Re ‘the rocks now referred to the Cambrian is Upper Potsdam, Lower
aE am, and St. Jolin’s group, and Newfoundland is cited as the local-
it y where the lower portion of the series is complete. The lowest, or
f t. John’s group, is correlated with that of St. John, New Bianawiok:
* “9 the Paradoxides beds of Braintree, Massachusetts. The lower
tsdam is represented by several hundred feet of limestones and

aa student’s manual of geology. Second edition. Edinburgh, 1862, p. 457.

_ eological survey of Canada. Report of progress from its commencement to 1863. Montreal, 1863,
3,11 plates. Atlas of maps and sections, with an introduction and appendix. Montreal, 1865, 9
and , sections.

Lacan, W. Bw. tien Silurian Rocks of North America. Geol. Surv. Newfoundland, Rep. Prog. for
gio 1866, PP. 45, 46. Revised edition, 1881, p. 49.

iy Ree gets ties THE CAMBRIAN.

sandstones on the Straits of Belle Isle, and on LW ati. Bay, Nowtiunds:
land, “and by the slates of St. Albans and Georgia, Vermont. ~The Up-|
_ per Botsdai is that of Wisconsin and Minnesota, represented in the —
typical Potsdam of New York. This horizon is not recognized in the - F
northern part of Newfoundland, but occurs on Conception Bay, inthe
_ southeastern part. The tabulation made by Logan has been followed
very largely by all writers upon American geology, and the succession — a
was not changed until 1888, when it was discovered that the St. John
group of Mr. G. F. Matthew was above the Lower Potsdam of Billings
and Logan. <4
The Geological sintres of N ewfoundland, under the direction of Dr. |
Alexander Murray, added materially to our knowledge of the Lower
Paleozoic rocks. All the strata beneath the Calciferous or Quebee
group were referred to the Potsdam group.' In the neighborhood of |
Canada Bay, on the east coast, the entire series referred tothe Potsdam —
has a thickness of 1,153 feet, of which the lower 700 feet belong to the
Lower Cambrian zone, as shown by Olenellus vermontana occurring in —
the upper portion.2. In the report of field work for 1868, Dr. Mur- — |
ray? describes the rocks about Conception Bay, in the southeastern =.
- portion of the island. Of the lowest bed exposed on Manuel’s Brook,a —
_ Sinall stream that flows into Conception Bay, he says: ‘¢On Manuel’s —
Brook a very coarse conglomerate may be seen, in strong and moder-
ately regular beds, resting directly upon the syenitic gneiss of the ;
valley above. * * * About 400 yards below the bridge the con- —
glomerate is overlaid conformably by a set of dark brown or blackish —
shales, * * * with some hard calcareous beds interstratitied,” and this
series extends down the stream nearly to the bay.* Dr. Murray also —
‘describes, ina section at Topsail Head, a gray compact limestone in —
strong solid beds, 1 to 2 feet thick, showing a vertical thickness of —
about 100 feet, together with some interstratined shale. The limestone |
‘is subjacent to a dark brown, finely laminated shale. Detailed sections —
are given of the shales and sandstones exposed on Kelly’s and Great —
Bell Islands, Conception Bay; the former has a thickness of 712 feet —
and the latter of 476 feet.- A summary of the rocks referred to the: —
_ Lower Silurian gives an entire thickness of 3,880 feet.° Figures of five ;
‘sections accompany the text, in which the anconformity- between the e
Lower Silurian rocks and the subjacent intermediate system or Huron- —
ian and the Archean is well shown. The subjacent slates and signal
Hill sandstones of Jukes are referred by Dr. Murray to the Cambrian — :
group on account of fossils having been found there, which Mr. Bill
- ings described as Aspidella terra-novica and Arenicolites. £ se

a

1Sequence and distribution of the rocks of the great Northern Peninsula. Geol. Surv. _New-
foundland, Rep. Prog, for 1864, Montreal, 1866, pp. 10,44. Revised edition, 1881, pp, 5-47.

2 Op. cit., p. 10. os

8 Of the seqnence and distribution of the formations. Report upon the geological murray of x ew- ; s
foundland for 1868, St. John’s, 1868, p. 68. Revised edition, 1881, pp. 154-167.

4 Op. cit., p. 154.

5 Op. cit., pp. 157-160. '
_S Op. cit., p. 144. , a —

_ : J 1 aes 4
- Cid

te | ; > a

os A rat = A
~ taker re) ‘s vines r, ~~, . , 5 -
SS ee s : my — ~ - °
4 in, ee ~ ; ;

- yt 2 mit. si a, i> , oe . 2 “, dy nn. G ~- i . ee.
"Seay Peer ee NEWFOUNDLAND. 53
a .

se the @ report for 1869 a description is given of the Lawet Paleozoic
‘s s studied by Mr. Howley as they occur on Trinity Bay and St.
MM: rye Bay. The variegated slates of Jukes are described as contain-
% “jng Paradoxes and the superjacent argillaceous shales and sandstones
% carry Cruziana and other fossils. These last represent the rocks of the
Bell Islands in Conception Bay. In the report for 1870? a summary is
~~ given of the then existing: knowledge of the Primordial formations in
& ‘southeast Newfoundland. In descending order the upper formation is a
R brown and black micaceous shale with the gray micaceous sandstones
Or Great Bell Isle, Conception Bay. The organic contents are: Two
> =: Species of Lingula, four species of Paleophycus, Hophyton linnceeanum of
- Torrell, another Eophyton and Oruziana semiplicata Salter. Thickness,
:. 476 feet. He says that the slates of Little Bell Isle and the beds of
‘shale beneath the water are considered to have a thickness of 1,426
feet, to which the Kelly’s Island sandstone and shale are to be added,
Rites thickness of 720 feet. [As now known this forms the upper.
x E aivision of the Cambrian.] Beneath this he describes the black slates,
See Paradowides bennetti, having a thickness of 150 feet. On St.
ry’s Bay this division, united with the red, green, and black shales
Pion slates, i in which Paradowides bennetti, Conocephalites gregarius and
oth er fossils were recognized, has a thickness of 1,045 feet. [This forms
_ the , middle division of the Cambrian as now Reon: | Below this the
2 hard. thick beds of gray and reddish limestone of Topsail Head, Brigus
- South Head, Conception Bay, and the Little Salmonier River of St.
a Mary's. Bay are united with various outcrops of red, green, and blackish
al gillaceous slates and a series of sandstones below. [These form the
Joy ower division of the Cambrian as now known.] The total thickness
| of the section described is 5,972 feet.? Several sections are illustrated
to show the ‘relation of the Primordial-Silurian to the subjacent rocks.
; = In the report for 1872 the Primordial-Silurian rocks are described as
they are exposed on Trinity Bay, etc., by Dr. Murray.t He states that
paleontological grounds Mr. Billings is disposed to draw a marked
dis inction between the upper strata of the section of 1870 and the
a wer members of that section, in consequence of an apparent hiatus or
aul in organic development between the Paradoxides beds and the
liferous strata of Great Bell Island in the Conception Bay section.
lower measures he [Billings] appears to regard as the equivalent of -
lower Lingula flags of Great Britain, or the Menevian group of
er and Hicks; while the upper parts contain forms in some degree
ical of the horizon of the’ Upper Potsdam.’ This is followed by a

hats, aware, Of the rocks and associated minerals [of Bonavista Bay, etc.]. Report
“ee geological survey of Newfoundland for 1869. Revised edition. 1881, pp. 200-203.

y, Alexander. Of Primordial, Silurian, and related formations. Geol. Surv. Newfoundland for
St. John's 1870, pp. 30-43. Revised edition, 1881, pp. 232-241.

5A E oe THE ‘CAMBRIAN. SE ae ee

_ the deposits on the islands of Conception Bay he says: ‘ From Mr.

_ and limestones of the Canadian survey. The observations made at these —

_ edition, Boston, 1883, pp.150-157.

list of the species described by Mr. Billings from the Paradoxides zone
_ and the strata of Great Bell Island.

rocks of this formation, come the Potsdath and Calciferous. There —

_ the Primordial beds of Newfoundland. This is shown in the chapter 4
on the “ Geology of Newfoundland,” where a summary of the geology —

ey Firat die eeE LIN Bee PO IS SOT Cg aa Mai Fn RET Byte Ge sei.
‘ re og a ier FY g - e- ~ Seer ‘he ero fete = we se Ns ale ips , > bates.) te
id re . ey ‘ ie > | . . ‘

a

+
= 4 z 27. tat Oe Se ise

Prof. John Milne traveled extensively along the coast of Newfouid-—
land, and published the results of his geologic studies in association
ith the “ Notes on Geology” by Alexander Murray.! The Primordial-
Silurian is spoken of as a separate division; then, superjacent to the 4

does not appear to be any additional data to that already given in the
report on the geology of Newfoundland by Dr. Murray.
When describing some fossils collected by Mr. T. C. Weston, of the:

a

Canadian Geological Survey, in 1874, from St. Mary’s, Trinity, and Con- —
_ ception Bays, Newfoundland, Prof. J. F. Whiteaves states that the —

paleontological evidence suatadiia the view of Sir W. E. Logan that the q
slates of St. John’s, Newfoundland, probably belong to the same horizon 4
as the Acadian or St. John group of St. John, New Brunswick.? Of

Murray’s report already quoted it would appear that the shales of Kel-. —
ly’s Island are not quite so old as those of Manuel’s Brook, but that —
they are older than the Menevian sandstones of Great Bell Island.”? _

Dr. Murray appears to have considered the Potsdam zone as above

._
*

is presented as taken from Dr. Manras? s work.‘ on
Prof. Alpheus Hyatt, in his expedition to Newfoundland, visited the —

north coast of the Straits of Belle Isle, and collections were made at —

Anse au Loup and Amour Cove from the “so-called Potsdam sandstones —

points indicate a fauna quite distinct from those of any of the limestones _
or slates of the west coast of Newfoundland. The absence of Cepha- —
lopoda and the prevalence of primitive forms of Archzocy athus show
the rocks to be probably older than those of the Quebec group at Port —
au Choix and other localities. The primitive sponges, or Archeocyathi,
have here replaced corals completely, and may be described as reef-
builders, since numerous hummocks and masses and parts of the strata —
are formed entirely of their remains. Immediately below these lime- —
stones, and conformable with them, lie the red sandstones, several .
layers of which are perforated with Seolithus burrows.” ®

A brief summary of the Lower Cambrian rocks of Newfoundland,
was given by Mr. C. D. Walcott, in a study of the Cambrian faunas of hy?

1On the rocks of Newfoundland. Geol. Mag., new ser., decade IT, vol. 4, 1877, pp. 251-262. re

2Qn some Primordial fossils from southeastern Wewdound ica: Am. Jour. Sci., 3d ser., vol. 16, 1878, 3 |
p. 225.

3 Op. cit., p. 226, 4

4 Hatton, Joseph, and M. Harvey. Geology of Newfoundland. Newfoundland, the oldest British colony, ‘=
its history, its present condition, and its prospects in the future. London, 1883, pp. 178-187. American :

5Expedition to Newfoundland. Boston Soc. Nat. Hist. Proc., vol. 28, 1886, Lae Cruise pe the’ a
Arethuss. Science, re 6, 1885, p. 386. i 7

. > + el > Re ee _ =. . seute en - . . or - ¢ . ad
. ree ee _ ae ; xe : ty oi
. Pe Spend : x 2ST ve & 7 Loe ’ . ete a ; * : - : ’

a ig NEWFOUNDLAND. == BB
th Aw rericat when disounetag the stratigraphic position of the Ole-
aon, In it he says? that the only locality known where the two
| pass occur in the same geographic area is on Conception Bay, New-
fonndland; and special stress is placed on the occurrence at Topsail
Head of several species of fossils typical of the Olenellus zone at the
PS traits of Belle Isle. This fauna was referred to the Middle Cambri ian,
although Dr. Murray states in his section of 1868 that Mr. Billings re-
ih erred. the species to the Potsdam.‘ By this Mr. Billings probably
meant his lower Potsdam, which is now (1890) included in the Lower
Cambrian.

i In an abstract of a ‘paper on the Cambrian faunas of Cape Breton
es pan, published in advance of the paper read before the

~ (1) The horizon of Paradoxides kjerulji.
Fares The horizon of the Conocoryphees.
_ (8) The horizon of Paradowides tessini.
_ (4) The horizon of Paradoxides spinosus.

- (5) The horizon of Paradoxides davidis.
2 Iti is stated® that “in this classification of the various Newfoundland
horizons in the Paradoxides zone Mr. Matthew has placed that of Para-
<. dox: des kjerul fi first or oldest, because that is its position in Scandi- |
ne avia.” In the final paper’ he speaks of the fossils found at Topsail
Head, and Brigus on Conception Bay, mentioning Agraulos strenuus,
Iphidea (allied to Iphidea bella Billings), and Stenotheca paupera Bil-
ings. He says these fossils do not give sufficiently firm indications to.
make it clear that they are older than some other horizons mentioned
reafter. He then describes the fossils of the Paradoxides zone. A
new v species, Solenopleura bombifrons, is described from the limestone of
| Topsail 1 Head.®
In the summer of 1888 Mr. C. D. Walcott made a careful study of the

t=
q\

1m nbrian section in Newfoundland, and determined the Olenellus zone

Piagon in his scheme of 1864. x: detailed section of the: Chimkerin
“strata on Conception Bay was published, with lists of the fossils
—-0€ seu irring at the different horizons in it.?

Second contribution to the siti on the Cambrian faunas of North America. U.S. Geol. Surv.,

‘the sequence and distribution of the formations. Report upon the geological survey of New-
land for 1868. Revised edition, 1881, ‘‘ P.1” of section, p. 157.
he Cambrian faunas of Cape Breton and Newfoundland (abstract). Can. Record Sci., vol. 2, 1886,

ae cit. 4. 258.
~-7 On : the Cambrian faunas of Cape Breton and Newfoundland. Bese Soc. Canada, Proc. and Trans.,
v stion iv, 1887, Pp. 147-157.

Nope, p. 156.

he stratigraphical succession of the Cambrian faunas of North America, Nature, vol. 38, 1888,
Pp . Stratigraphic position of the Olenellus fauna in North America and Europe. Am. Jour.
Sei. 3d ser.,. vol. 37, 1889, pp. 374-392 ; vol. 38, 1889, pp. 29-42.

eee

_ = tiny Tests yas a Oe

BS i ae aap ‘THE. CAMBRIAN.

oe big cc Sirs ee “NOVA SCOTIA. Pe Ste Se

=

~The altered or metamorphic uate belt of the Atlantic coast of No ova. |
_ Scotia is represented on an early geological map by Dr. Avraham Ges-
ner! as extending from Cape Canso to Cape Sable. He states thatthe —
area is within the primary district and composed principally of granite, —
gneiss, and mica slate. A general description of the rocks is given in
the account of the local geology of the townships in which they occur. —
At a meeting of the Geological Society of London on May 10, 1843,
Dr. Gesner? presented to the society a geological map of Nova Bootide 3 :
accompanied by a memoir on the geology. In the text? the lowermost —
of the Silurian rocks devoid of animal remains is referred to the Cam-
brian. The map was not published with his paper. It appeared in. —
18454 in connection with papers by Mr. Richard Brown, on the geology —
; of Cape Breton, and Mr. J. W. Dawson, on the Lower Carboniferous
7 rocks or gypsiferous formation of Nova Scotia. The strata new pro- | a
visionally included in the Cambrian group are indicated on the map

~~. as micaceous and chloritic slates, clay slate, quartz_rock, and graywacke —
slate. They extend entirely around the central area of granite and —
syenite, and are separated from the Atlantic coast by a broad belt of
_-color designated as granite. Ata later date Gesner described the strat- —
ified non-fossiliferous rocks or Cambrian group of Nova Scotia® as ana a
extended belt of hornblende slate, chlorite slate, clay slate, graywacke —
slate, and quartzite, succeeding the granite and its associates, and with —
them occupying almost the whole of the Atlantic side of the province. —
No fossil remains have been found in any of these metamorphic masses. —
-_In 1850 Dr. J. W. Dawson described the Atlantic coast series as fol-
-.. lows:

os

\

é
= 8

~

The prevailing stratified rocks in this group are compact and flaggy gray quartz- —
ite (often weathering white), mica slate, and clay slate, the latter usually of dark —
colors, and occasionally passing into flinty slate and quartzite. * * * 4

The hypogene rocks associated with them are white and flesh-colored prahiber “g
which has penetrated the metamorphic rocks in large irregular bands and masses. os

As a result of his study of this group of rocks Dr. Dawson concluded |
Ss that they belonged either to some of the older members of the Silorian |
S system or to a still earlier period. In the first edition of the Acadian —
, Geology Dr. Dawson stated that the rocks are certainly older than the - |
= Devonian ; and he was inclined to believe that they represented the —
Potsdam sandstone and Utica and Hudson River shales, in an altered —
condition.?7, On the accompanying map their geographic distribution —

1 Remarks on the geology and mineralogy of Nova Scotia. Halifax, N.S., 1836, pp.272. +f a
2A geological map of Nova Scotia, with an accompanying memoir. Geol. ae mma antc Proe., vol.
4, 1843, pp. 186-190.
3 Op. cit., p. 187, '
4 Geological Map of Nova Scotia. (Accompanying papers by J. Ww. Dawson and Richard E Brown.)
Quart. Jour. Geo]. Soc,, London, vol. 1, 1845, oppo., p. 23. 4
_ 5 The industrial resources of Nova Scotia. Halifax, N. S., 1849, pp. 233, 234. : ae
® On the metamorphic and metalliferous rocks of eastern Nova Scotia. Quart. Jour. Geol. Soc., Lon:
don, vol. 6, 1850, p. 348. - ~ 7 See
Acadian Geology, 1st Edition, Edinburgh, 1855, p. 357. . - a '

i
a.
= .

a “ = _ Nova puetia, = 55-3 oe

8 } n”? a.

I Ina a sipplementary chapter to the first edition the slates and quartz-
pe ites of the Atlantic coast belt are spoken of, and it is suggested that
S y may’be a continuation of the Primordial zone of Newfoundland,
“it n which Paradoxides have been found.! Mr. E. Billings reviews this
_ supplementary chapter and says: “We are strongly inclined to the
- lief that this supposition will yet turn out to be well founded.”
an In 1862 the slates of the Nova Scotia metamorphic slate belt were
_ referred to the Taconic System.2 A more detailed description of the
ae ks was published by Dr. J. W. Dawson, in 1868, in which they are -
ated to be formed of granite, gneiss, mica slate, quartz rock or quart-
- “zite, and clay slate. The granite appears to be intrusive, and the gneiss
: is considered a product of a metamorphism or baking of sedimentary
Tot ck: . The clay slate or argillaceous slate abounds, and is usually,
€ along: the Atlintic coast, of a gray and black color, varying very much
‘in texture and hard nias,* He states that the series has not afforded
- fo »ssils, but it appears to be a continuation of the older slate series of
M Be B. Jukes in Newfoundland, which has afforded trilobites of the
onus: Paradoxides. On the map accompanying the volume the geo-
gre phic distribution of the series is clearly exhibited.

In a general description of the Nova Scotia gold field Mr. J. Camp-
bell publishes a section across the gold-bearing rocks of the Atlantic

-
i

coast, in which the arrangement and relative position of the different
gro aps of strata are well shown. There is a great thickness of quartz-

t Sepieoeat to blue and gray slates divided midway by the “black
rock.” Very few details are given of the section, as the report is
ai ink devoted to a conus ea of mining and the mode of occurrence

T
5

. Whe B Rite citine upon the Waverly gold district Prof. H. Y. Hind
i Ee ad that he had found Paleotrochus minor and Palewotrochus major of
Emn mn ons, besides numerous concretionary forms, in the Waverly beds.
He considers (a) that these fossils, if identical with those from North
0 ina, probably establish the age of the gold-bearing rocks of Nova
Scoti ia; (b) that they occur near the base of the Lower Silurian System ;
{© that they belong to the upper part of the Potsdam formation and
1 ower part of the Calciferous formation, and (d) that they are sub-
t to the great mass of serpentine and red slates, discovered by
lo eeseran in Antigonish, which belong to the Quebee group. The
Series is correlated with that described by Dr. Emmous in North

Ag

plem entary chapter to the Acadian Geology, Edinburgh, 1860, p. 53.
ew of) Acadian Geology and a Supplementary Chapter thereto. Canadian Nat., vol. 5, 1860,

cou aieten. [The slate of Nova Scotia, metamorphic Taconic rock.] Boston Soc. Nat. Hist.,

4

I. 9, 1862, p. 47.
in Geology. The geological structure, organic remains, and mineral resources of Nova Scotia,

\

A

ie I etl
“—

-

%

~~,

y

58 CS ge eee - THE CAMBRIAN. a’ Peat ani ‘

- of stratified gold-bearing slate and quartzite, stating that all former ob-

series. His first impression of them was that they represented the

tous slates at the Oven’s Bluffs numerous specimens of the genus”

' supposed to be the equivalent of the Laurentian system. Halifax, N.S., 1870, pp. 14.
~ 5Q0p. cit., p. 8. Se

So ee ES ae Se Be eae Se cies as Ca On eer en

a at oe; mt Nagy ae a Oe Sere a aay, To 2 ee Fas eS

~ : oS : = > 45 yr . a s

: ; ar a, hae A as ‘ —_ ‘ zy . nts : .
Ben hs ; 3 re oe '

“4

“ .
Carolina.’ In a paper ee to the igeblozion Bodiety of London,? 4
and subsequently published in the report on the Sherbrooke gold dis-
trict of Nova Scotia, Prof. Hind describes the gold. bearing rocks of
Nova Scotia as follows: . a 4
~ The gold-bearing rocks of Nova Scotia are of Lower Silurian age, rare either —
on Huronian strata or, where these have been removed by denudation, on the old g

Laurentian gneiss. The gold is found chiefly in beds of auriferous quartz of con-—

et

temporaneous age with the slates and quartzites composing the mass of the series, ,
which in Nova Scotia is 12,000 feet thick, and the auriferous beds are worked, in one —
_ district or another, through a vertical space of 6,000 feet.® . om
Ina report on the gneissoid series underlying the gold- bearing rocks —
of Nova Scotia the same writer‘ states that he has provisionally referred -
the gold-bearing series to the Lower Silurian, but that conclusive ev i-
dence derived from fossils has not been obtained from the gold- bearing aj
slates and quartzites. Since the discovery of the forms resembling the —
Paleotrochus of Emmons, noticed in his report on the Waverly dis.
- trict, he has sent to Mr. Billings slabs containing supposed fossils from
the Sherbrooke rocks. Mr. Billings thought that a species: of ‘Orthis —
and an EKospongia were indicated. In describing the gold- beanie
rocks under. the head of “ Lower Silurian” Prof. Hind® Says : rf ht
The known gold-bearing rocks of Nova Scotia consist of quartzites, sandstones, 4
and grits, interstratified with argillaceous slates and thin conformable beds of aurif- —
erous quartz. This portion has an ascertained thickness exceeding 9,000 feet. * *— 4
The thickness of the black slates in Nova Scotia exceeds 3, 000 feet, so that the gold-
bearing rocks of the province have a known thickness of 12,000 feet. . :
The essential parts of the description in the last paper are also
- printed in the American Journal of Science.®
In his report on the gold fields of Quebec and Nova Scotia, Dr. A. 3
R. C. Selwyn’ speaks ofthe geological position of the Atlantic coast series ©

servers are agreed that they probably belong to the Lower Silurian —

groups known in Britain as the Harlech grit-or quartzite, and the —
Lingula-flag series. He discovered in the gray sandy and flaggy pyri-

Eophyton, and states that Mr. Billings regarded this genus as charac- —
teristic of the Primodial Silurian epoch. He then gives an account of
the distribution of the genus Eophyton, and in conclusion says: “ In

1Report on the Waverly Gold District, with geological maps and sections. Halifax, 1869, a 61.
2On two gneissoid series in Nova Scotia and New Brunswick, supposed to be the equivalents of the ~
Huronian (Cambrian) and Laurentian. Quart. Jour. Geol. Soc., London, vol. 26, 1870, pp. 468-479.
* Report on the Sherbrooke gold district, together with a paper on the gneisses of Nova Scotia and
- an abstract of a paper on gold mining in Nova Scotia. Halifax, N.S., 1870, p. 3. NZ
4Preliminary report on a gneissoid series underlying the gold- teeta rocks of Nova 5 Seotia, and

i

6 On the Laurentian and Huronian series in Nova Scotia and Wav Bpanawille Am. Jo our. Scei., 2d ry
vol. 49, 1870, pp. 351-353. ;
- 7 Notes and observations on the gold fields of Quebec and Nova Scotia. Geol. ‘Surv. Canada. Report L
Prog. for 1870-’71, 1872, pp. 268-270. » :

- ? ~~ a x

re oe a. ee ;
ce 4 a tin ~~ “ns

+ tee » es : \

’ et ere

a al aspect, and in ne succession of the beds the whole series ‘in

No ova ‘Scotia in the supplement to the second edition of the Agadian
cology? and places the slates and quartzite in the Cambrian. He
ites that the evidence of fossils in determining the precise age of these
ks is unfortunately as yet somewhat imperfect, and quotes Prof.
lind as saying that the entire thickness of the series is 12,000 feet;
of this the lower or quartzite and slate division comprises about 9 000
fee et, and the upper or ferruginous slate division about 3,000 feet.

c* 3 a one
| -=S @ .
es

a Er
o to

fr om near the Morthenxetrn point of the peninsula south to Sable River,
‘ where they are interrupt ted by a mass of granite that extends to Har-
73 rington Harbor. From this point around the western slope to Annapo-
nh is@a sin. they occupy a wide strip along the shore. As represented on
i A “map they occupy nearly one-half of the area of Nova Scotia.

mn 1888 Sir William Dawson reviewed the rocks referred to the Cam-

ova a group on the Atlantic coast of ak : ae that the Atlan-

ap a eared to. rest on rocks of Huronian aspect. He also says: )

It has unfortunately afforded no well- characterized fossils. The markin gs called
yton and certain radiating bodies gail ant gpsnaes pound in it aati Powe sim-

er to be regarded as a great development of the lowest member of the Cambrian,
a cag gerated equivalent of the Harlech grits and Llanberris slates. In this case,
however, = may be ‘expected that it will yet afford true Cambrian fossils.4

*. *

‘ NEW BRUNSWICK AND CAPE BRETON.

Epsncr® uses the term “Cambrian system.” He says:

name has been applied to a group of rocks situated beneath the “ Silurian ”
from which it is not always separated by any very distinct line of demarca-
far as its lithological character is concerned. The few organic remains, how-
found in this group are sufficiently characteristic to make it appear that the
of animal life during the period of the accumulation of its strata were different
hose found in the upper Silurian rocks.

= eee
— —

104 Dp. eit, ay Pp. 271. .
*Supp lement to the second edition of Acadian Geology, containing additional facts as to the geolog-

u uctare, fossil remains, and mineral resources of Nova Scotia, New Brunswick, and Prince
Island, London, 1878, pp. 81-83.
16 Eozoic and Paleozoic rocks of the Atlantic coast of Canada, in comparison with those of
Europea and of the interiorof America. Quart. Jour. Geol. Soc. London, 1888, vol. 44. pp. 804-807.
K ord of Science, vol. 3, 1888, pp. 182, 183, 230, 231.
ey) P. 805.

i on the spenieeieel survey of the Province of New Brunswick, with a topographical account

ie aes NEW WavRewise AND CAPE BRETON, 59. .
a -

: “On the colored geological map of the Dominion of Canada, pub-
1 shed i in 1882, the Cambrian rocks of Nova Scotia are made to extend

g gard this Eination as Sieiduiding to his Sareiaak=s in Newfoundland; but it~
s not agree with this either in mineral character or in fossils, and is perhaps»

}

i

SG Ss SESE “THE CAMBRIAN.

\

- mentioned by Dr. Gesner are, however, now included in the Cambrian a

* Cambrian are distinguished from those of the Silurian by their ery

‘principally to the map prepared by Dr. Robb. Of the rocks he says: —

The rocks of this group extend fro the nati boundary line and cross ‘hes b
St. John a little above the Meductic, and proceed in a ners direction toward
Bathurst. * * *— - : ; : ga

The strata consist chiefly of grauwacke, grauwacke slate, and clay dint: The vada
wacke may be compared to a very compact sandstone. There are also beds of con- —
glomerate, containing bowlders and. pebbles of almost every variety of rock. The ~
cementing matter is generally calcareous or argillaceous; but it is sometimes silicious, ©
and the beds change imperceptibly into quartz rock. The slates-are of different —
colors; red,blue, and green are often seen. Many of them contain lime, and others .
will supply roofing slate. ee

>
a

-The local details of the distribution of this series are not given, nor ;
is the locality of the city of St. John mentioned. Portions of the rocks

group. 7 ze
In his third report Dr. Gesner! recognizes two series of rocks, both —
of which are referred to the Silurian age. The upper group consists of —
limestones, slates, and sandstones, containing the remains of plants, —
mollusks, ete. The older group is formed of conglomerates, gray sl, eS,
sandstones, talcose Slate, and the vay beds of Mispeck and lack.
Rivers. > Sia
On a map prepared by Dr. James Robb, * the geographic distribution 4
of the formations described by Dr. Gésner is outlined, and under the ©
‘¢Qambrian system” we find the indicated distribution of the Cambrian —
rocks to include Carboniferous, Devonian, Lower Silurian, and Cam-
brian as now known. In the text of the volume accompanying the map 3
Mr. J. F. W. Johnston* describes the geographic distribution of the —
rocks and also their general character. He states that the rocks of the a
hardness and by their containing less lime. }
In speaking of the rocks referred to the Lower Silurian and Came
brian, by Gesner and Robb, Mr. J. W. Dawson‘ states that for the dis- —
tribution of these rocks, as indicated on the map, he was indebted

I do not think that at present there is any good ground for separating the so- called | j
Cambrian rocks from those last mentioned [Silurian], though it is quite probable that
they may belong to an older formation, or that they may be older members of the
same formation. S , te

When relating the results of a visit to New Beumbwick Prof. Ww. |
B. Rogers® described, by the aid of a section, the stratigraphic features
exhibited at the junction of the older and less ancient groups of strata
on the St. John’s and Kennebecasis Rivers, a few miles above the city ~

1 Third report on the geological survey of the province of New Brunswick. St. Jobn, 1841, pp. BAL. 4

2(Letter on the geological structure of New Brunswick.] Report on the agricultural “snes
‘of the province of New Brunswick, by J. F. W. Johnston. Fredericton, 1850, pp. 12, 13. =e

% Report on the agricultural capabilities of the province of New Brunswick. Froderictos, 1850, PP. ;
17, 18.

4 Acadian Geology, first edition, 1855, pp. 324, 325. =

*Remarks on the geology of the neighborhood of St. John, New Brunswick. Boston Soc. Nat,
‘Hist. ,Proc., vol. 7, 1861, p. 176. P

~~

ah Se SU a Sy oe EN ret tp a a ‘ee?
a om eee, _ .-.~ p 4

ALC mh aoa “NEW BRUNSWICK AND CAPE BRETON. _ 61
a ae ;

$i John, as observed by Dr. Robb and himself. Referring to the
able ages of the two groups he states that the only fossils discov-

ee and some black scale-like fragments of aivelia that he found
bout the city of St. John in loose pieces of siliceous slate. At several
points s the layers of rock in piace are crowded with these remains, the
x re entire of which presented the form and markings of a Lingula.
ae r. J. W. Dawson described in 1862 the strata about St. John, and
pu blished a section! that includes the shales and slates of thé ianits
of ‘the city; and, in the same section, a series of beds which have since
Dr proved to be of Devonian age. He states that the age of the lower
mel mn bers was less certain. They may represent either the Middle and
I ower Devonian, or may be in part of Silurian age. ‘The only deter-
nable fossil, the Lingula of the St. John shales, affords no decisive
¢ one of tiie question.”
1 In pereyesis g a classification for the pre-Devonian rocks of New Bruns-
, Mr. G.' F. Matthew? states that Gesner’s older group is to a
great eH extent younger than his upper series. He reviews the classifica-
‘ion of f Dr. Dawson? dividing the formations into several groups; pro-
it g the name St. John group for Nos. 5 and 6 (in part) of Dawson’s
on of 1862. He says that the St. John group is formed of several —
mn a of soft, black, dark gray, finely laminated shales, alternating with
1es of coarser gray Slates, containing numerous thin beds of fine-
grai ed sandstone, the whole having a thickness of about 3,000 feet.
Phe fossils noticed were a Lingula, a Conchifer, Anuelids and Coprolites.4
the Coldbrook group, No. 6 of Dawson, in part, is given a thickness of
a ) feet or more composed of greenish gray slate, bright red slaty
D lomerate and dark red sandy shale, with a reddish conglomerate,
and hard, gray sandstone. The paper is accompanied by a map
10 wing the geographical distribution; also a section crossing the dis-
in the vicinity of St.John. In a foot-note mention® is made of
scovery of numerous trilobites of two or three species, but they
80 peaneseively distorted that the genera could not be made out.

a5

L, W. Bailey ° reprinted the table of formations published by Mr.
ow in 1863. Ina table on page 14 he places the St. John group
» base of the Lower Silurian as an equivalent of the Potsdam or
‘dial of New York and the Quebec group of Canada. A full de-

a

lon of the St. John group is given,’ and accompanying it a letter

Finca of the Devonian period in northeastern America. Quart. Jour. Geol. Soc. London, vol.

ions on the geology of ethete New Brunswick. Fredericton, 1865, p. 8

“

"setts; ; with the Paradowides bennetti beds of Newfoundland; the Lin- ©

es ry : ot ps Cea Pe AMS gy be
aX , sf 2 2 ‘x tees &
62- ss ore oy “THE CAMBRIAN. x i‘

apparently new, the occurrence of Paradoxides and Conocéphalites led _
Mr. Hartt to correlate the entire fauna with the Primordial fauna of Bar-.7 rs.

the Chazy. Thesubjacent Coldbrook group is referred to the Huronian, —

‘St. John slates, the Acadian series®> In 1868 he republished all the facts —

‘John group.?

~

from Mr. C. Fred Hartt, 1in which he states that he his eobenlacd four
genera of trilobites from the St. John rocks, viz, Paradoxides, douse
cephalites, Agnostus and a new genus (?) allied to Conocephalites. 7
There are also six species of Brachiopods, belonging to the genera Or- —
thisina, Discina, Obolella, and Lingula. Although all of the species are —

rande. He states that the lower part of the St. John group, at Cold- —
brook, has been divided by Mr. M atthew, ‘on pena ic) grounds, into —
three bands, viz:

No. 1.—The lower or arenaceous band, with no pethticnt fossils, and con- q

stituting passage beds from the Coldbrook group. .
No. 2.—Argillaceous shales, rich in fossils, Paradoxides, Orthisina ?, Conoceph- —

alites, Obolella. ~ - -
‘ No. 3.—Carbonaceous shales, full of fossils, Paradoxides, Conocephalites, Or- a
thisina, Discina, ete., all much” distorted. : A

In the same year Mr. G. F. Matthew described the Azoic pas of |
southern New Brunswick.? He gave the geographic distribution of —
the St. John series, and a detailed section of the formation, to which he —
assigned a total thickness of 4,500 feet. He mentions the identification —
of the fauna by Prof. Hartt; ane refers the St. John group to the Lower —
Silurian, correlating it with the Paradoxides harlani beds of Massachu-_

gula flags of Great Britain; the alum-schists of Benridinaeste and —
‘‘Ktage C” of Barrande in Bokeraie He states that the upper por- |
tion of the section may be the equivalent of the Calciferous, perhaps —

while the terms Cambrian and Huronian are used as synonyms in their
application to the Coldbrook formation.‘ o

In noticing the discoveries made by Messrs. G. F. Aatihew and C, KF
Hartt, Dr. J. W. Dawson refers to the correlation made by Prof. Hartt,
and proposes to call this series, represented in New Brunswick by the ~

known to him in relation to the St. John group, naming it the Acadian —
group, and including it under the Lower Silurian.® The section given
by Mr. Matthew is published, and also descriptions by Mr. CO. F. Hartt _
of all the Sees discovered by Messrs. Matthew and Hartt in the St

1 Preliminary notice of a fauna of the Primordial period in the vicinity of St. John, N. B. Obser- 3
vations on the Geology of southern New Brunswick, 1865, pp. 30, 31.
2On the Azoic and Paleozoic rocks of southern New Brunswick. Quar. Sant Geol. Hoes London, —
vol. 21, 1865, PP. 422-434, map. ate SS
3 Op. cit., pp. 426, 427. —-

4 Op. cit., p. 427.
5 On recent geological discoveries in the Acadian provinces of British poner Am. Assoc., Proc.
vol. 16, 1867, p.118. Canadian Nat., new series, vol. 3, 1868, pp. 295-297.
6 Acadian Geology. The geological structure, organic remains, and mineral resources of Nova a Scovel
tia, New Brunswick and Prince Edw. Island, London, 1868, pp. 637-641, 2d ed. ae. cig
7 Op. cit., pp. 641-657. Te an

Uietc 4 ie fe ie _ . > . > wth< o> te ee ff

oie es oly bevxswic AND CAPE BRETON. | 63

SN
9 n 1860 Messrs. Matthew and Bailey’ described in a general maiiner
oe e rocks referred to the Lower Silurian and stated that this series in-
cludes a about 150 feet. of slates (holding Paradoxides, Conocephalites,
Agnostus, and other trilobites, besides several genera of Brachiopods),
a and an overlying mass, measuring not less than 2,000 feet, of flags and
. slates containing Lingule, worm burrows, ete. Under thé caption of
& « Lower Silurian,” the same writers, three years later,” include the St.
John or Acadian group. A brief historical sketch is given, and a list of
. fossils that have been described from the formation, with a statement
Bh at the apparent thickness of the whole formation, as measured in the
- city of St. John, is about 4,500 feet. Owing to the disturbed condition of
th e beds the actual thickness may be much less. If repetitions occur,
_ the aggregate thickness of the series, exclusive of the lower red beds—
= | hich have been called Upper. Coldbrook—will not much exceed 2,000
fe et. This general description is followed by a detailed one, and a
opy of Mr. Matthew’s section at the city of St. John The St. John
group is then described as found in the Kennebecasis Valley, in north-
; 8 rn King’s County; in Wickham, Queen’s County; in Nerepis Valley,
2 and in Charlotte County.
<n. the supplement to the second edition of Acadian Geology, Dr. J.
W. . Dawson* introduces the term “Cambrian” and includes under it the
sh eadinn series of St. John and also the great Atlantic coast series of
Nova : Scotia. ‘ Nothing is added in the way of descriptive details to
th ose given in the edition of 1868.
| & D uring the survey of the island of Cape Breton, Mr. Hugh Fletcher 3
a scovered near Marion Bridge, on the banksof the Mira River, aseries
is ght gray, slaty, fine-grained, feldspathic sandstones, associated
with an and green mottled sandstone in which he found numerous
pecimens of Obolella. He points out the lithologic resemblance of
e rocks to the Primordial rocks found by Mr. Alexander Murray in
t outheastern part of Newfoundland and to those on the Strait of
Belle Isle examined by Mr. Richardson.’ He also describes a series of
Ir ‘ple, red, and green slates, sandstones, and limestones, that he refers
‘the Ewer Silurian.? A detailed section of the rocks is given as they
ar along St. Andrew Channel. In one of the greenish and blue
ery slates he found impressions of an Obolella, with the head and

of: a trilobite, recognized by Mr. Billings asof Primordial or Quebec

al ars on the age and relations of the metamorphic rocks of New Brunswick and Maine. Am,
Proc., vol. 18, 1869, pp. 182,183. Can. Nat., new ser., vol. 4, 1869, pp. 326-328.

reliminary report on the geology of southern New Brunswick. Geol. Surv. Canada, Rep. of Prog.,
7 1, 1872, p. 134.

Op. cit., p. 135.

4Op. cit., pp. 136, 137.

~ p| ement to the second edition of Acadian Geology, containing additional facts as to the geolog-
neture, fossil remains, and mineral resources of Nova Scotia, New Brunswick, and Prince,
I Island, London, 1878, p. 81.

ort of explorations and surveys in Cape Breton, Nova Seotia. Geol. Surv. Can., Rep. Prog.

gf. *

are given of the St. John group.

basins or trough-like depressions among the older hills of pee 4

_ He repeats this correlation a year later,’ when he says: “ Prof. Hartt —

' Brunswick. Geol. Surv. Can., Rep. Prog., 1877-’78, 1879; p. 28DD-34DD.

sh | ale Ps , =e ae nes
64 ra “THE “DEVONIAN “AND - CARBONIFEROUS. wee oer oy
ae FAT RPS ‘ . 3h

Lor te /
group age. In bis report for the flteeing year he! described a num 4
ber of sections, referring them to the Lower Silurian, and mentioning — |
the occurrence of Lingula, Obolella, and Dictyonema in some of ‘the —
beds. ,
In a report on the slate formation in the sorthess part of Charlotte -
County, New Brunswick, Mr. G. F. Matthew? states that the St. John — |
group occurs in the interval between the Kingston or Upper Silurian —
rocks and the inclosing Laurentian ridges in Kin g's County. No. deta a

A report on the Primordial-Silurian rocks of Hew. Brunswick by Mr. :
L, W. Bailey? presents a detailed description of the St. John group. AD :
section is given of the strata on Ratcliffe’s Mill-stream and Handford —
Brook and local details of geographic distribution. This is accompanied —
by a list of the fossils found which were identified Se Mr, J. F. Whit
eaves.
In a later report on the geology of southern New Brunswick! the 4
Cambrian or Primordial Silurian rocks are described as occupying

rocks east of the St. John River. : +3
In speaking of the strata carrying the Paradoxides in the anuiees
of the city of St. John, Mr. G. F. Matthew® states that the strata of |
the St. John group fill a number of narrow, trough-like basins lying —
between the Bay of Fundy and the central Carboniferous area of New —
Brunswick. A carefully measured and detailed section of the St. John —
outcrop is given with a description of the conditions under which the ’
fossils occur in the same. A thickness of prea feet i is seainnne see ice ;
section. ae)
The same writer argues in a paper on the “Geologie Age of the_ 4
Acadian Fauna”® that on the evidence of the trilobites the St. John
group does not quite correspond to the Menevian of Wales, in the re-
stricted application of that term; but, as a whole, they indicate the sub- ~
jacent Solva group as the eieaie: formation to the St. John group. —

fixed the age of the St. John group as nearly as was possible in- his time 4 3

“4

1 Report on the geology of part of the counties of Victoria, Cape Breton, and Richmond, Nova nena
Geol, Surv. Can., Rep. Prog. for 1876-77. Montreal, 1878, pp. 429-437.

2 Report on the slate formations of the northern part of Charlotte aac New Brunswick. Geol.
Surv. Canada, Rep. Prog. for 1876-77. Montreal, 1878, pp. 342, 343.

3 Report on the pre-Silurian (Huronian) and Cambrian or Primordial Silurian rocks of southern Now 4

‘Bailey, L. W., G. F. Matthew, and R. W. Ells. Report on the geology of southern New Brruawiaed
embracing the counties of Charlotte, Sunbury, Queens, Kings, St. John, and Albert. _ Geol. Surv. aay {
Rep. Prog., 1878-1879, 1880, pp. 6D-8D.

5 Illustrations of tha fauna of the St.John group. Royal Soc. Canada, Proc, and Trans. vol. 1, sec.
iv, 1883, pp. 81-88; pp, 271-279.

6The Geologic Age of the Acadian fauna, The Primitive Conocory phean. British Assoc. Rep., sith 4
meeting, 1884, pp. 742-743, The Geologic Age of the Acadian Fauna. Geol. Mag., new ser., decade, 3.
vol. 1, 1884, pp. 470-471.
5 7 = outline of recent discoveries in the St, John group. New Brunswick Nat. Hist. Soc. Bull No

y 1 p. 98, .

pe Yate tae 2h apie on a ie EO! COE ef ee Be Le ee eg
ey} “ yh te —S Z - a < eg Ee > t¥ + hy ce

Fan < ake F = 7” he ; :
ee: - Re hase 3 4 2

m0 ordial, ? or, as we now call it, Cambrian.” He then calls atten:
» article i in which he saereiatod the St. John group fauna with
4 group, stating, “Tn other words, it is the fauna of the older

3 In a Ratisinary study of the Cambrian fauna of North America! a
review is given of the history of the term “ St. John group” by Mr. ©. D.

d ? and all species described by Mr. C. I’. Hartt in the second edition
of J Dawson’s Acadian Geology were illustrated.

= Ww hen discussing the faunasof theSt. John group, Mr. Matthew? states

tha hit is lughly cnpacnaes me the group covers nearly the whole of the

iat. of the shallow. water eens bbal St. John group near the sum-
Sa the series. The’ vad poodles by Mr. by Stes in the Cam-

it hew? to belong to the Olotius division of the Fasbietas fauna. The
ies recognized by him are Peltura scarabeoides, Spherophthalmus

| ft LS paper appeared in the Canadian Record of Seidics. vol. 2, 1886,
p. 255-258. i

ly of the red rocks beneath the Paradoxides zone. These strata
een spoken of as the upper member of the Coldbrook group® and as
st tuting a series lower than the Primordial rocks at the base of the
an... They were subsequently joined to the St. John group® as the
jase Of that group. In a later report in 1888, Mr. Matthew’ says: “ It
S no\ w found that this red series is unconformable, not only to the St.
m group, but also (as had been previously discovered) to the under-
es BORD. In the valley of Long sett: of ie St. John

» Cambrian faunas of North America; preliminary studies. U.S, Geological Survey Bull. No.
1884, p. 289, separately paged, p. 9.
strati ons of the fauna of the St. John group, No. 4, Can. Ree, Sci., vol. 2, 1887, p. 362. Pees

et “ ‘NEW / BRUNSWICK ‘AND CAPE BRETON. ae 65 |

c ott. In this the use of “ St. John” was advocated as against ‘“‘Aca-

is, and Agnostus pisiformis. In the same paper he mentions the —

estes zone in Sweden and Russia; Mr. Matthew‘ began anew the >

fo and in the variousbeds. These include trails at casts of marine

LZ

SS Sh PRA IE 2 Pee Hear), se se F OR OE eR I
x . ~ ; - 7 mat

f atl Pie ie > DAS hes Syl ate
t . oy “y ‘ . ‘ at z = od: - i 2 et pees bate tak :
ee Se eA THE CAMBRIAN. 8S PRY oe Ce ie .

Tee
aeaa: bacica: and an siikocagieed Ricekuanea: This aber was fol.
lowed in the same year by an article on the classification of. the Cam- |
~ prian rocks of Acadia in which the classification of a Cambrian sys:
rom in Acadia and Newfoundland is given as follows:* a

Series A.—The Basal series or Eteminian.
Series B.—The St. John group or Acadian.
Series C.—The Lower Potsdam or Georgian.
Series D.—The Potsdam sandstone and limestone.
The division of series A was noticed in the preceding paper = Mr.
Matthew. In series B he includes the zone of Paradoxides ; describes _
the rocks in detail, and gives lists of the genera of the ey a) Series” q
C, the Lower Potsdam of Billings, he states has not been recognized on —
the mainland of Acadia, but is found in the Island of Cape Breton, _
where the fossils are Bathyurus, Orthisina, Orthis, Hyolithes princeps.
This series is placed provisionally above B.2 Series D, or the Pots-—
dam series of New York and the Mississippi Valley, is stated to be ab-
sent from New Brunswick and, as far as known, from the eastern
border of the continent. ? a
A reclassification of the Cambrian rocks of North America was pub--
lished in 1888 by Mr. C. D. Walcott as follows :4

TABLE I.—Lower Silurian (Ordovician) system.

ae

Subdivisions. Terranes. Faunas.
Upper Cambrian ............. | Potsdam, Knox, Tonto, Bell Isle, ete .......... Dicelloce phal u s or
«| Olenus. . | 2 oie
Middle Cambrian............. St. John, Avalon, Braintree ...... sesccescacces Paradoxides.
Lower Cambrian™.\..<...-<2.. Georgia, Prospect, Terra NOva:<i-<Gennasnass Olenellus.

x i

This is followed by a comparison of typical sections of the Cambrian
system in Sweden, Newfoundland, New York, and the Rocky Mountains. -
The section on Manuel’s Brook, Conception AS Newfoundland, where
the true stratigraphic succession of the Cambrian deposits in America )
was first discovered, is given in detail. | —

- On learning of the discovery of the Olenellus fauna beneath the
Paradoxides zone in Newfoundland, Mr. Matthew published a second
paper “On the classification of the Cambrian rocks in Acadia,” it in
which he arranged the Cambrian system as it occurs in Acadia | as
follows :° . Se

Localities. a
D. Upper Cambrian (Potsdam series) .2 352. sncdec cccuce ence ucctd cccces Unknown.
C. Middle and Lower Cambrian—Acadian series ......-..--..-------- St. John, otal
B. Lower Cambrian—Georgian series ...... 2-222 40-22 sees cone ee ee -. Cape Breton.

A. Basal Cambrian—Etcheminian series .........-...----..- pon Ree . St. John, ete.

‘ ‘Matthew, G.F. On the classification of the Cambrian rocks of Acadia. Can. Ree. ‘Sei., , vol. 3, 108, 3,
p. 72. E
2Op. cit., pp. 73-74. 3 Op. cit., p. 80. Sat
ke stratigraphical succession of the Cambrian faunas in ‘North America. Nature, vol. 38, 18

5 is the classification of ihe Cambrian rocks in Acadia. No. 2, Can. Ree Sci., a) 3, 1889, p30,

f -

x ae
es.
Ay P,

ting comparisons ebesay: the sections of Sweden and New

Sok, he discusses the general yelations of the Cambrian fauna

orth America. The organic remains found in band B are an

aulos, and at the base of the zone an Hllipsocephalus, of the type

: ciated with Olenellus (2) kjerulfi in Europe. At the base of band B-
fe ound aspecies of Obolus which he described as Obolus pulcher.!. This:

nprises the Lower Cambrian fauna or pre-Paradoxides fauna as

kn own to him from New Brunswick up to date.

an another paper on the ‘Cambrian orgabisms in Acadia,” pub- —
ishe ed in the same year, he notes the discovery in the lower beds of the.

,
|
i

; oe Section, beneath the Paradoxides beds, of several varieties of

ponges, a species of Paleochorda and another undescribed species.
Undoubted ESumpies of Platysolenites oe Pander also oceur,? Men-

hi Eicoet under the title of Peltura beds, correspondin gin age to the
Ci ape Breton Upper Cambrian beds.

In September, 1889, Mr. Matthew? argues for the uniting of the
Ole enellus or Lower Gambian) and the Paradoxides or Menevian zone,

ons

a ~

$s one division of the Cambrian, and the strata above the Paradoxides ~
“zone as the upper division, thus returning to the classification of Salter.
and Hicks, adopted for the Cambrian strata of Wales.

- The full text of Mr. Matthew’s paper on the Cambrian organisms in |
Ac adia was distributed in June, 1890. It deals almost entirely with
the pre-Paradoxides or Basal series of the Cambrian section of New
unswick, and is accompanied by both tabulated and illustrated sec-
ns and sketch maps of Hanford Brook and Caton’s Island.* It is
red to at length in the description of the Cambrian rocks of New
Brunswick in this paper (Chapter. Iv).

In a paper read May 28, 1890, Mr. G. F. Matthew gives a detailed
ita of the geologic structure of the St. John basin in connection

unswick.®
In a list of the a logiesl formations of the Maritime Provinces of
mada, Dr. George M. Dawson tabulates the Cambrian as follows:

: pper Cambrian ie: a Miré and St. Andrew series, ~
es 7 sx BOS ee MRS Eg Cape Breton.
oe MINE este eo. ke op wha eee Acadian series.

Atlantic Coast series.
Nova Scotia.

he Cambrian organisms in Acadia. Can. Rec. Sci., vol. 3, 1889, p. 384.

is the Cambrian divided? A plea for si classification of Salter and Hicks. Am. Geol., vol.

Pp. 139-148.

ambrian organisms in Acadia. Trans. iy Soc. Can., vol. 7, sec. 4, 1890, pp. 138-143.

thew, G. F, Illustrations of the fauna of the St. John group, No.5. Trans. Roy.Soc, of Cones ;

ec. 4, 1891, pp. 123-130, pls. 1-XVvI. 5s
American Geological Railway Guide. J. ame sMcFarlane. 2d ed., 1890, p. 52,

i, *» ~ w

-

stated that the correlation was more from fancy than real argument, 4

‘as smoothly and even gracefully curved semi-cylindrical grooves and

{*- he = Te ay i ~~ ne! * res ¢ 563 7 = AM ee 4 + eet f +
- -* —h “ a eat Ts <a x one
i ‘ : ¥ . ‘ Sy 4 ‘S < - % 7 _~ see oi ae, st A TAL
Ma eas ey Pee nrg Cree et = oR I cae
68 x are van gt CAMBRIAN. af MRR te

¢ MAINE.

- When describing the quartz rock of Bar Harbor, Mount ‘Desert _ 4
Island, Prof. C. 8. Hitchcock! suggested a Lower Silurian age for the
siliceous slates associated with the coarse sandstone or quartz rock,
by comparison with similar rocks on Flint Island, of which he ‘hed

because it reminded him so much of the Potsdam sandstone in its ex.
ternal appearance. | . ' a
At a later date he says :? ; ae e
The first rock is a sandstone at Bar Harbor, dipping at an angle of twelve degrees.
Ripple marks cover the surface of many layers, and curious cylinérical stems tantalize

~

us by their resemblance to fossils. The formation is probably of Cambrian age. — eZ. a

a

The strata included under the title of ‘‘Cambrian” about Portland, P
‘Maine, is described by Prof. Hitchcock * as follows:

These rocks crop out in Saco, a dozen miles west. They are clay slates and indu- —
rated argillaceous schists, the latter having a northwest strike, while the rocks of the —
older series run northeasterly. These rocks are in character and position allied to —
the Cambrian Paradoxides slates of Massachusetts, and exist in immense mass 8 along
the coast of Maine west of Saco, and in New Hampshire. =

The correlation of these beds is based entirely upon their lithological |
characters, as no mention is made of any fossils having been found i in |
them. a. |

In his account of the geology about Frenchman’s Bay, on the coas |
of Maine, Dr. W. O. Crosby describes the slate formation. The pre-—
vailing rock is a compact and well jointed argillite or clay slate, of
black, drab, and purple tints, with distinct stratification. The author
concluded that these rocks are the newest rocks on this part of the
coast, by their relations in dip and distribution to the present contours ~
of the land; by their unerystalline character; by their relations to the
intrusives ; : ~~ the fossils which they cantatas The latter he describes _

ridges about a line in diameter; they are often a foot or two in length, — .
and might sometimes be ropariel as annelid trails, but in other cases —
they are irregularly branched in a way that would be impossible with
worm-grooves, but is very suggestive of smooth, slender fucoids.4 The
general conclusion feached was that the Frenchman’s Bay series Dbe- ©
longed somewhere between the top and bottom of the Cambrian, with”
the chances in favor of its being near the latter. In other words, his
observations tended to corroborate the suggestion made by Prof. Hiteh- | |
cock twenty years before. He further states: a

1 Reports on the Geology of Maine. Second annual report on the natural history and geology of
Maine. Augusta, 1862, pp. 269-271. <

?Gevlogy of New Hampshire. Concord, 1877, vol. 2, p. 32.

>The geology of Portland. Am. Assoc. Proc., vol. 22, pt. 2; 1873, p. 168, s

4Geology of Frenchman's Bay, Maine. Boston Soc. Nat. Hist., Proc., vol. 21, 1881, pp. 111-116.
of Frenchinan’s Bay, Maine, just east of Mount Desert Island. Am, Jour, Sci., 3d ser., wah ae 1882, p- 64,

»

esem blanco of these rocks to ‘ie: Acadian slates of the Boston Basin and St.

ta n “deserib ng a sbaidiie map of “Maine, Prof. Hitchcock says that he
eit to divide the Cambrian and Huronian, owing to a want of ©

i owled ge of their distribution.

‘They are thé talcose and mica schists of the reports, called the Gaver group by
h Y. Hind and Sir W. E. Logan; the St. John’s group in New Brunswick, and the
Merrimack, Rockingham, Kearsage, Andalusite, and Cos groups of the New Hamp-
e reports. * * * They were called Cambrian in New Brunswick by Gesner,
lin our second report it was said that this term might ultimately express their.
age. Subsequently Bailey and Matthew referred them to the Lower Devonian
but the drift-of opinion is towards the earlier view at present.? — .

z Bos the map it is very difficult to make out the distribution, owing to
t © color, of the Laurentian, Silurian, and the Cambrian ‘vole appa-
1 nuy identical. The supposed Cambrian rocks of New Hampshire
and southeastern Canada follow up the valley of the St. John River
om a little distance above the entrance of the Allegosh River, and
al ong the Canadian boundary line nearly to the boundary of New
Ae mpshire. The Canadian extension of these rocks is described more
n detail and will be mentioned under the head of the Canadian Exten-
| oa of the Northern Appalachian District (Chapter Iv). _

In the latest contribution that we have upon the subject of the geo-
J rival age of the siliceous slate and page sandstones or quartz

en limestones ghows that thet are no limy eniei in the sedimentary deposits of —
s island. The aggregate thickness of the various Mount Desert sections can not be
than about 6,000 feet and may amount to one-half more than this estimate. It
s as if this fact must exclude the hypothesis that these strata were formed any-
€ 8 in ane periods above the level of the eaeieg for nowhere above that level

Itm may be next noted Saaseitine the schistose series of Mount Desert that those of
ei east and west margins are of singularly uniform composition. They were doubt-
originally shales and thin sandstones of great uniformity of structure. Their
re sis. not such as at all points to exclude the preservation of fossils; indeed the
ter portion of the deposits are well fitted to exhibit organic remains, yet they
ve é fforded no trace of them. Nowhere above the level of the Cambrian series do
} ind any section of this description. On thease grounds, it seems reasonable to

=
aa : Sy ue. miss = . : : >
ue: E ‘ y : i

a+ a : 2
. oan A | r= 4 -
> o, >* « ae . .
oe - a r

Dr. C. T. Jackson describes the Cambrian system as understood by him 7

' They were supposed by Dr. Carr, who first noticed them, to be graptolites, which are y

- serrated fossils have a great vertical range in the older or protozoic rocks, being found —

By {| anbte ears ‘(ME CAMBRIAN. oA a eee
; > - : Pig o ry < y: -
: NEW HAMPSHIRE. — A Re ate Se i <

Pr the final report of the geology and faieeealeoe of New Hampshire, ”

at that time, and states that metamorphic Cambrian rocks. occur in t
New Hampshire, but they contain no fossils. He also says: ee:

The oldest transition, or Cambrian rocks, occur in Maine and Vermont, and d dip 1
opposite directions, indicating an anticlinal axis in New Hampshire. ;
On-the eastern side of this axis we discover the first distinct fossils in the slate
strata on the Kennebec River, where the strata dip boldly to the northwestward. a
On the western side we have not yet determined the limits of the Cambrian fossils,
but indistinct remains of organic substances, whose nature is problematical, occur in —
the neighborhood of Castleton, and along the western flank of the Green Mountains. 4

supposed to be allied to sea-pens. Graptolites are described by Murchison as belong-
ing to the lower part of the Silurian system. He states, however, that these pen-like —

from the lower part of the Ludlow formation down to very ancient beds in the Cam-— “a
brian system. ;
Should these fossils prove to be eraptolites, they would indicate the proximate limits 7
of the Cambrian rocks on the western side of the New Hampshire anticlinal axis,
where the strata dip to the southeastward. =
It will be observed that the strata become more and more renead as we proceed
eastward and westward from this axis, as is proved by order of superposition, am
logical characters and fossil contents of the rocks. 1s

Prof. Hitchcock says? that the term adi brian is ; misapplied by Dr
Jackson, and the ideal section showing the structural geology is incor-—
rect in many of its details. In the final report of the second 7 eoloriodil
survey of New Hampshire he describes the Rockingham mica-schist as”
an uncouth mica-schist. The Merrimack group is a micaceous quartz-—
ite that has not yet been fully separated from the previous group. It
abounds in beds of coarse, indigenous granite, which seem to have been, |
altered in situ from the feldspathic conglomerate. In certain parts of
Strafford County the granite beds predominate, forming numerous hills, —
while the slate occupies the valleys between.? Some schists with inter :
bedded clay slates which are referred to the Merrimack group, are ang
posed to be equivalent to the Paradoxides beds of Massachusetts. _

The Connecticut Cods period can easily be divided into three parts: first, the ep och
of the deposition of the inountain masses of silica; second, of hornblende and mica
schists; third, of limestone. -

In the White Mountain region there are severa) small areas of andalusite slate ay 4
supposed to be the equivalent of the Coés group. * * * * The Cods period was —
terminated by eruptions of syenitic granite. * * * * The Coés quartzite —

constitutes a distinct range of mountains.® 3 ¥ a

The Mount Mote conglomerate is formed of an eruption of igneous
material cementing together the slaty fragments. This is included i in the e

1 Final report on the geology and mineralogy of the State of New Hampshire, with contributi ons
towards the improvement of agriculture and metallurgy. Concord, 1844, p. 14. a a
? History of the Geological Surveys in New Hampshire. Geology of New Hampshire, vol. 1, 1874 »P- a
8 Physical uistory of New Hampshire. Geology of New Hampshire, Concord, 1874, vol. Jd, Be: 536,
4Op. cit., p. 587. 5 Op. cit., p. 538. . “apa
fea

* aie: a a
Race the ardhian Sad the ian. Giibd. On ‘hed map
D “page 536 the formations referred to the mica-schist period are
y: outined. In a subsequent paper Prof. Hitchcock! presented a
le or scheme representing the stratigraphical column of New Hamp-
i: The Cambrian includes at the summit the Rockingham schists,
below, in order, the calciferous mica-schist, the Cods group, clay
ites, and Mount Mote conglomerate. The description of the various
formations is given on page 13 and on the map the geographic distribu-
tionis delineated. This paper appears to have been prepared and pub-
lished prior to the issue of the second volume of the Geology of New
;, ead and it does not refer to the volume. On page 674 of the
er work the formations in New Hampshire are epee as follows:

. ' Feet.
( Upper Helderberg eFerinone) 200; Lower Helderberg, 500...-.. 700
| Calciferous MsGh GONISG 5 22. nd aes enstessdasck~s gacd 6 agate
Pale ses DU MROMCE-GIATO a. hoi 5 ey aeons bay sce eeebaw ats 3, 000
ae e ¥ Cods group. Mica schist, often stauroliferous ..............-..- 3, 300
i . EATER ss SOs Se ate foc Spon clu cceoes ebdacue?s 1, 000
Cambrian slates (Connecticut Valley)...... ......---2-. ses. --0. 3, 000
, Total Paleozoic...... ee Sh cP Soo ois Zn, wh Siu, Splat - 15, 800
ae r meeeearae Anaalusite STOP i... )2. os... 42252... scene pow wta cane 1, 300
_.__| Rockingham mica-schist..-......-+-...---+-----++22ee0 +--+ cet CORE
4 eonoie? 2 INNIS EOIN in a wale Sy anid wow Ue wks we nos eee occe Bene wones 4, 300
ae ; | Ferruginous slates, with steatite (probably repetition of preced- Ss
sae a Ee ee Beeret se pean eb tase’. ik canes debt rep
A RINNE CR LO, Ok ns mn an doe cain ade de caeendes 3% 1}, 600

ns iader. the head of Pcpcaee, in the Geology of Northerd New
E ngland, Prof. Hitchcock says :°

. % The. discussions about the value of the Cambrian series are leading geologists to
sign to this place i in the column a thick mass of sediment, usually without fossils
a largely argillaceous in character. We may for the EG place here the follow-
ng yroups: (1) Mica-schists of southern New Hampshire. (2) Merrimack group,
including argillo-quartzites in Coés County. (3) Cods group. (4) Clay slates. (5).
nt Mote conglomerates. J

r

cin | | one of his later Peper, Prof. Became) ‘in speaking of the various

ed to aa Rei Moplasl as aks ancient or on the verge of the
“he an a table giving the thickness of oe formations °. the

aa C.H. Geology of Now Hanhenhics, Concord, 1877, vol. 2.
Port map | of New eens and Vermont, with notes on topography ina geology. In Ge-

“a

t, BP. 178, ui,

ie ee erga at Sn gis an RCN ae a ICT
ae is eRe eR RSA _THE _CAMBRIAN. Goma a.
we find the Crystalline group that. was referred to the Cambrian in the
Geology of Northern New England in 1874, as follows: eer it oa
‘ Crystalline group. be
apm Feet.
Calciferous mica-schist and Coés group ...-....---------+ --eeee oe ee eee Ne ~ 12,000 —
5 Kearsarge group... . .scas one oe sedeee dn came essen totems eeagen wie sen aie 1,300—
Rockingham mica-schist......--------- Sree re Pe ee Pag 000
WMETPUOO CK: COUP. o<.2c.0csco+atanae sacs ch senna aie Phe eal eye Sanbedice ieee

-

Beneath the Merrimack group the eure is placed, with a thick.
ness of 12,000 feet. | .
. - In a tabulation of the geological formations of Maine, How. Hamp:

shire, Vermont, Massachusetts, Rhode Island, and Connecticut, by
Prof. Hitchcock,! the calciferous mica-schist, staurolite slate and schists, —
quartzite, andalusite schists, and Rockingham mica-schists are in- a
cluded in the Cambrian. In a foot-note he says that the quartzite, —
staurolite slate and schist, and the calciferous mica-schists may yet
prove to be Silurian. In his classification of the Paleozoic rocks of —
New England he places under Cambrian the St. J ohn or Aran slate,
Taconic slate, and Roxbury conglomerate. are my

In a table published in 1890 he includes only the Potsdam, Georgia, | 4
Acadian, and the Taconic slate (in part) in the Cambrian. All of the — :
foliated erable rocks of New England are classified as preCam: 9
brian.” | |

~

EASTERN MASSACHUSETTS,

The references to the argillite and limestone in which the Cambrian —
faunas have been found, in the Boston and Narragansett Basins, occur —
in most of the publications relating to the geology of eastern Massa- —
chusetts. In 1818 Messrs. J. F. and 8S. L. Dana stated that the argile
lite was the oldest rock known in the region.’ Its distribution is shown —
in a general way upon the map accompanying the report. It is stated
to be subjacent to the syenite in Milton and Braintree, and to ke
stratified. In the works of Prof. Amos Eaton‘ the rocks of easte
Massachusetts are shown in sections, but nothing is added to the data
given by the Messrs. Dana.

The next description of the geology of Boston and vicinity, by Dr.
J. W. Webster,’ mentions that the light gray clay slate is the only rock —
found on the Boston Peninsula in situ. He noticed the presence of the

; slate in Quincy and also at Nahant. : a

} Maine, New Hampshire, Vermont, Massachusetts, Rhode Island, and Connecticut. (aaulbienl for. fo -

mations.) Macfarlane’s Am. Geol. R. R. Guide, 1879, p. 56. oh. 44

*Idem., second edition, 1890, p. 86. ~~

3Ouwilines of the mineralogy and geology of Boston and its vicinity, with a geological map. Am, -

- Acad. Arts and Sciences, Memoirs, vol. 4, 1818, pp. 129-223. ~ a

4An Index to the Geology of the Northern States, with a transverse section from Catskill Mountain —

: tothe Atlantic. Leicester, 1818, pp. 52. A Geological and Agricultural Survey of the District Ad

joining the Erie Canal, Albany, 1824, pp. 163, plate.

> ®Remarks on the geology of Boston and its vicinity. Boston Jour. Phil. and Arts, vol. 2, 1824, pee
* —.. 2Ti-292. =

ity Sesion, oud seated that the unstratified rocks were of igneous
origi in and intrusive among the stratified rocks. A general description
s argillite is given in the text with localities, and on the map the
raphic distribution, as known to him, is delineated. This includes
the Sie In the final vate of the Massachusetts survey

Dawaet cas of Riidestsisch, liane small bed of compact light

ras limestone occasion the red sandrock. He did not see much of it
? meee, but the numerous blocks in the stone walls indicated its ex-

Bianca in that locality. On the map accompanying the report the ar-
eous slate i is shown in eastern Braintree, the central part of Quincy,

ace extends across, Milton and Dorchester to Roxbury. A small

ater op is also indicated on the north side of Nahant. The North At-

—

rough locality of the Cambrian as now known is covered by the
poniferous (No. 17 of the legend of the map). The description in

oe Ria an article on the beiiniaetiing fepestoues of North America. DeF:
3. Hunt? suggests that the limestones interstratified with the red slates
Attleborough, as described by Dr. Hitchcock, may correspond to
| a Bewhick with ‘similar slate and sandstone are ae with at the base
| Carboniferous formation in Canada and in New Brunswick.

| long silence in relation to the geologic age of the altered rocks

f Bete Massachusetts i in the vicinity of Braintree was finally broken.

n 1856 by the announcement of Prof. W. B. Rogers that trilobites of

20US and argillaceous slate lying on the boundary of Quiney and
tree, about 10 miles south of Boston. In announcing this discov-

3 He states:*

c Sep ae

The Koki in which these fossils occur is a compact, dense, rather fine-grained, sili-

=

ya Haceous slate or slaty sandstone, containing little or no carbonate of Rises.

oS _ * One of the most curious facts relating to the trilobite of the Quincy
i aintree belt is its seeming identity with Paradowides harlani, described by

nhis] Monograph of North American Trilobites.

1 ;on the geology of Massachusetts, examined under the direction of the government of that
ing the years 1830 and 1831. Am. Jour. Sci., vol, 22, 1832, pp. 1-70, with map.

eport on the geology of Massachusetts, 1841, vol. 2, p. 537, Amherst.

Sci., 2d ser., vol. 18, 1854, p. 199.

the Protozoic age of some of the altered rocks of eastern Massachusetts from fossils

Ss covered. at Acad. Proc., vol. 3, 1856, p. 317.

‘compares the species found with Paradovides spinosus of Bar-

report of 1841 is essentially the same as in the preliminary report of |

venus Paradoxides had been discovered at a quarry in a belt of

*

‘See i er 7 ae Bees
< i Pe Pee Nai dS ; fi et . bs ; mks Lt 6D
74 “THE CAMBRIAN. Ais “wee

He wide farther: |

The occurrence vf well preserved fossils among rook so highly alteked and 80 con-
tiguous to great igneous masses as are the fossiliferous slates of Quincy may walt
encourage us to make careful search in other parts of New England where heretofore _
such an exploration would have been deemed useless.! ;

Prof. Louis Agassiz, in commenting upon the announcement of F Prof. Pe
Rogers, said that, geologically speaking, its importance could hardly”
be overestimated. We have now, he remarked, a standard level upon
which to build up the formation of the metamorphic rocks. Prof.
Rogers also communicated the knowledge of the discovery of the—
Braintree fossils to Prof. J. D. Dana, in a letter dated August 13, 1856.°
He states that his attention was called to the locality by Peter Wain
wright, Esq., who resided in the vicinity of the quarry. ‘

Dr. Isaac Lea‘ visited the Braintree quarry, and in reporting upon it
to the Philadelphia Academy of Natural Sciences stated that he
agreed with Prof. Rogers in placing this formation among the more
ancient of the Paleozoic periods. ‘It lies directly on the granite rocks,
or rather it is squeezed in, and is embraced by these rocks (on the east
and west sides), which are disturbed by an upheaval.” He considere d
the trilobite found there to be undoubtedly the same as described by”
Prof. Green many years before under the name of Paradowxides harlani.

Prof. W. B. Rogers again called attention to the Braintree locally
for the purpose of noting the fact that the formation was among the
oldest of the Paleozoic series, ‘and situated somewhere about the level
of the Primal rocks (Potsdam sandstone and the Protozoic sanitolll
of Dr. D. D. Owen), containing Dikellocephalus i in Wisconsin and Min- :
nesota. B: .

In 1856 Prof. C. T. Jackson ® described the rock at Bratntrea as a
blue gray, argillaceous slate, containing silicate of lime but no carbonate a,
and some disseminated iron pyrites. The stratification of the rock, as Ss
indicated by its grain and cleavage, dips to the north 50°, and runs east
and west. The existence of the genus Paradoxides in ihe argillaceous Ss
slates of Braintree, proves them to belong to the lowest of the fossiliferous
Silurian rocks, and he believed them to be the geological equivalents
of the argillaceous slates of Sweden, which are in a similar manner dis
rupted by the intrusion of syenite. | . = nea .

1 Am, Acad., Proc., vol. 8, 1856, p. 318. 2Tbid., p. 319.

3Discovery of Paleozoic fossils in eastern Massachusetts. Am. Jour. Sei., 2d ser., wel: 22, 1858, Po
296-298.

4[On the trilobite formation at Braintree, Massachusetts.] Phila. Acad. Sei., Proe., vol. 9, 1858,
p. 205. - an

5(On trilobites from Braintree and on the geologic relations of the district.] Boston Soe. is
Hist., Proc., vol. 6, 1856, pp. 27-29, 40, 41. > f

6 [On the Hirniniebs argillite and its trilobites. ‘J Boston Soc, Nat. Hist., Proc., vol, 6, 1856, pp. 244,

“

- i. 2h, gis Roe ve me ek ga re YP * i. “es a ae: a Ee ee
eae Ss ~ ian Nl ee ea RY 2-l on
ee (a5, > on = 4 : . f =
aa soohiy
(ee
or. pee WF _-BASTERN MASSACHUSETTS, 15
‘ te oe -

tr bites i in the Silurian and Bitchin:

_ Prof. W. B. Rogers sent to Mons. J. Barrande? a photograph of the
Paradoxides found at Braintree. Barrande compared it with Paradox-
ide es spinosus-and concluded that Paradoxides harlant was a synonym of
ce Paradoxides spinosus. ;

In 1861 Prof. Rogers® announced the discovery by Mr. Norman Eas-
ton of pebbles carrying fossils of the Potsdam fauna in Carboniferous
¢ conglomerate north of Fall River, Massachusetts. He thougit the forms
a ‘ istinctly recognized in the pebbles were Lingula of two species, resem-
bling Lingula prima and L. antiqua of Emmons, from the Potsdam sand-
stone of New eta and that the rocks from which the peuee were.
; Braintree Beeciicitie beds. The conglomerate i in which the pebbles
occur is considered to be of Carboniferous age.

Bey ations communications were made to the Boston Society of Natural
ory respecting the Paradoxides fauna at Braintree, by Messrs.
fules Marcou and ©. T. Jackson in 1861 and 1862. From. that time
until 1869 little attention appears to have been given to the Braintree
ro Jn the latter year Prof. N. 8. Shaler‘ described the rocks in the
5 vi cinity of Boston, and referred to the argillites of Braintree, stating
at they were deposited in deep water. In 1870 Dr. T. S. Hunt ex-
ined the rocks near Braintree, and stated that the unaltered argil-
lites of Braintree, holding the Primordial fauna, were observed by Prof. |
Sha ler and himself to rest directly upon a hard porphyrite felsite of .
he e ancient series.. He says:°®

ue The fact that the Primordial strata of Braintree have suffered no metamorphism is
more significant, since the beds of similar age in New Brunswick and Newfound-

est unconformably on crystalline strata supposed to belong to the same ancient 7 .
ies that underlies the Braintree beds, and are, like sas unaltered sand and mud ~

~

1875 Mr. W. W. Dodge’ described the rocks at and about Batik
ein the Boston ‘Basin with great detail, and accompanied this with

in ae same year, in some remarks on Massachusetts geology, Dr. T.
Z Hunt? reaffirms his observation on the relations of the fossiliferous

Catalogue of State cabinet and notes on metamorphic rocks] 6th annual report of the Secretary
wchusetts Board of Agriculture, ete., by Charles L. Flint, Boston, 1859, p. iv.

rilobiten der Primordial-fauna in Massachusetts. Neues Jahrb. fiir Mineral., 1860., pp. 429-431.
O1 fossiliferous pebbles -of Potsdam rocks in Carboniferous c nglomerate north of Fall River,
chusetts. Boston Soc. Nat. Hist., Proc., vol. 7, 1861, pp. 389-391.

the Telations of the rocks in the vicinity of Boston. Boston Soc. Nat. Hist., Proc., vol 13, 1869,

1e geology of the vicinity of Boston. Boston Soc. Nat. Hist., Proc., vol. 14, 1871, p. 48.
jaa the geology of eastern Massachusetts. Boston Soc. Nat. Hist., Proc., vol. 17, 1875, pp.

#
ar
a. -
sah “
a> a a
. v4

_of Massachusetts, and said:! oe ie

chusetts, with its accompanying map, appeared in 1880. He Says: Sa

16 Sle os wee oe |THE CAMBRIAN.- ex basta: Tas

“more than one locality affording fossils. ‘This is the celebrated slate quarry: of the

rocks of Braintree and St. John, New Branswick, to hee sub
erystalline Huronian strata. pra. :.
The following year Prof. W. O. Crosby described the Geological May D

” & a

- Although the fossils characteristic of the Acadian group ae been found at only
one locality in Massachusetts, viz, Hayward’s quarry, in Braintree, yet most obra
eis agree that the greater portion of the slates in the vicinity of Boston are probably
of Primordial age; and I have so represented them on the map. oy

%, +e
The strata referred to are then described in a general way. 3 "a
‘In 1875 Prof. W. B. Rogers? announced the discovery of impressions -
suggestive of the fossil Lingula mentioned by him from Fall River, in
pebbles of the conglomerate, at Newport, Rhode Island. The pebbles ;
consist of a gray siliceous rock or quartzite.
The memoir of Prof. W. O. Crosby on the Geology of eastern Massa-

The Paleozoic rocks of eastern Massachusetts occur, as already indicated, only i in-
limited basins or depressions excavated in the ancient crystalline formations. . .— re
The most diligent search, continued for many years, by, in the aggregate, a smal 2)
army of observers, has failed to bring to light, among the rocks of the Boston Basin, |

south shore of Hayward’s Creek, in the extreme northeast corner of Braintree. 2. eo

- essentially conformable series; although (p. 186) there is in the Boston

texture are very compact and highly crystalline or saccharoidal. These iS

‘underlies the latter. From this it follows that the slit is of. Primor-

- Boston Soc. Nat. Hist., Proc., vol. 21, pp. 274-277, 1882. - 2 a

Prof. Crosby‘ concludes that the Paradoxides ‘bed in Brain-
tree is the established base line for the stratigraphy of the Boston _
Basin; and that all the rocks in the Boston Basin above the Shawmut |
group, and including the Paradoxides bed, belong to one and the same

Basin essentially but one conglomerate and one slate, and the forme) ri

dial age, and the conglomerate must be of the same age, or older. a?
conglomerate is stated to pass gradually into the slate, and a detailec
description of these two formations is given as they occur in the Bostal
Basin. On the map a part of Nahant is colored to indicate the Cam-
brian slate. In the text he describes white and gray limestones that in ~ .

have a thickness collectively of perhaps 20 feet. He assigns to
conglomerate a maximum volume not exceeding 1, 000 feet; and con 4
siders that the greatest thickness of the slates canted be ash less thar ie
that of the conglomerate, though in some eases falling below 500 feet.>

Dr. M. E. Wadsworth,® in discussing the relation of the Quiney eran
ite to the Primordial argillite of Braintree, states that Dr. Hunt wai

1 Report on the geological map of Massachusetts, Boston, 1876, p. 40. tees An
?On the Newport conglomerate. Boston Soc. Nat. Hist., Proc., vol. 18, 1875, p. _ 100. ~ ae
%Contributions to the geology of eastern Massachusetts. Boston Soc. Nat, Hist., Oceasional pape p
No. 3, 1880, p. 181, 183. : F
4Op. cit., pp. 184, 185. 5 Op. cit., p. 266. Sdketan .
On the relation of the Quincy granite to the Primordial argillite of Braintree, Massachuse e tts.

Se aS ara aa ee pag eee oe ehh RAAT * Pb Way
ee Se ue pips ia aaa - * 3 5 re
s ae Ae ge sed ieee ald tics Maes Nia Se NOR REIN
2 eet. hy 55 3 ;
aa ee "EASTERN MASSACHUSETTS, ieee 3

x4 pe o%,

) ding itas a ‘metamorphosed sedimentary rock. He says the
te is surrounded by intrusive granite of a later age, thus adopt-
fae advanced by Dr. Hitchcock in 1832. In deseribing the

=~ ea its structural seicwete: ~~ another paper, published
following year, Dr. Wadsworth discusses the argillite and conglom-

tl ere | are at least two distinct argillites. One like that underlying the
lomerate on Beacon street, Boston, and resembling in some of its

ser er erain, often more decidedly arenaceous, and generally of a gray,

al the 1e argillites and the schists of allied character. Of these we only know the age ©

ery small area in Braintree and Quincy. * * * Older rocks than the Brain-
(Paradoxides) argillites may exist, but of their existence we thus far have no

ou cca of Rasbeian rocks in eastern Waa mcirddeties He describes
‘geographic distribution and the character of the rocks, and in an
mpabying paper in connection with Mr. A. F. Foerste gives a deserip-
1 of the fauna. As the description of the strata and the fauna
hat which is given in our summary of the present knowledge of the
ks of eastern Massachusetts, it is here omitted.

8 review of the stratigraphic position of the Olenellus fauna by.
zD. Waleott in 1889,* it is, shown that the Paradoxides fauna of

Ss

. ‘This is SS uariied more fally. in a paper in thes Tenth Anbost
rt of the Director of the U. S. Geological Survey.’

n a sketch of the physical history of the Boston Basin, Prof. W. O.
y' mentions the old and more or less altered or sinitemuak phic slates

» Braiutr ee quarry, and states it to be clearly established that the

argillite and conglomerate of the Boston Basin. Boston Soc. Nat. Hist., Proc., vol. 22, 1883,
oe Pp. 132, 133.

a College, vol. 16, 1888, pp. 13-26.
raphic position of the Olenellus fauna in North America and Europe. Am. Jour. Sci., 3d
ol 37, 1889, pp. 374-392; vol. 38, 1889, pp. 29-42.

2 of the Lower Gainbrian or Olenellus zone. 10th Ann. Rep. U.S. Geological Survey, 1890,
) 3, plates 49-98. Ps
sical nase of the Boston Basin. Lowell free lectures, 1889-1890. Boston, 1889, pp: 22,

‘inregarding thoaninite as Gf Huronted age,.as was Prof. Shaler —

ite of the Boston Basin,!' and concludes from studies made by him that.

aracters the Paradoxides argillite si Braintree. The second is of z

geology of the Cambrian district of Bristol County, Massachusetts. Bull. Mus. Comp.

Bs AO a Bae ae Ngee a POO ee Fe ee ee ae ae RERUN po Sete ee big:
; ‘ 2 7 ——_ ‘ a eae ACs + * egal 2 Xa a ns ad " Cory ’
OE RE ee gO. Nn eee a a wy ie be "iE ae ae
pa . We oy tae Sake Lf mr. S a \ a ee
73 Ra Se a THE CAMBRIAN. USNS Ete BEY cco 81.
a - 1 2) ee oe mes .

‘granite: is ocuptive iiduigh, and Giesefate newer (Sat the Primordial
slate. The evidence of the trilobites shows that the slates were formed
me. very far back in geological time, and near the base of the recognized
: : - geological formations. In a résumé of the geological history of the
- _ Boston Basin,'a general description of the Primordial slates and quartz.
_ ites and their physical relations is given. of
_ In mentioning the discovery of fossils in the limestones at Wana Mr. 4
“A. F. Foerste correlated the Nahant limestone with the red slates of
- North Weymouth, and concluded that they are stratigraphically beneath
- the Braintree Paradoxides beds, and that the red slates of Mill Cove at
North Weymouth are of Olenellus age and beneath the Panos
strata.” .
| In 1889 Mr. A. C. Lane described the geology of Nahant from a miner- |
me — alogical standpoint, Sand in the following year Prof. J..H. Sears pub- 4
lished a description of the stratified rocks of Essex County, which in- 4
cludes the limestones and associated slates of Nahant. He mentions
finding Hyolithes princeps, Hyolithes communis var. emmonsi, Hyolithes im-
-_ par, and Stenotheca rugosa.s He also discovered an outcrop of the Lower
‘ Cambrian limestone in a valley between Prospect Hill and Hunslow’s
Hill, in Rowley, in which fragments of Hyolithes occur.

~~

PALEONTOLOGY. oe

NEWFOUNDLAND.

The first announcement of the discovery of the Cambrian fauna in~
Newfoundland appears to be by Mr. J. W. Salter® in the description of
Paradoxides wir 3p He gsi. are species to the “ Lingula flags or
Zone Primordialé.”™” ee

From collections made by the Canadian Geological Survey Mr. B.
Billings described in 1861° the fauna from the Cambrian strata on the
_ * north side of the Straits of Belle Isle, on the Labrador shore, at TAnse |
au Loup, and assigned it to the horizon of the ‘‘ Lower Potsdam,” corre-
_ lating it with the fauna found in Franklin County, Vermont, which i is”
; described in the same paper. The species described are Paleophycus
| ineipiens, Archeocyathus atlanticus, Obolus labradoricus, Obolella chro-
matica, O. (Kutorgina) cingulata, Conocephalites miser, Bathyurus senectus,
B. parvulus, Salterella rugosa, 8. pulchella, and 8S. obtusa. The new

1Qp. cit., pp. 19-22.
; 2 The Paleontological horizon of the limestone at Nahant, a a Boston Soc. Nat. Hist.
x Proc., vol. 24, 1889, pp. 261-263.
3Geology of Nahant. Boston Soc. Nat. Hist. Proc:, vol. 24, 1889, pp. 91-95. Bae
4The stratified rocks of Essex County. Essex Institute Bull., vol. 22, 1890, p. 32. a
5On the fossils of the Lingula flags or ‘‘ Zone Primordiale. ” Quar. Jour. Geol. Soc., Leta vol
_ 15, 1859, p. 552. 3
6Paleozoic Fossils, vol. 1. Containing descriptions and figures of new or little known species « of
organic remains from the Silurian rocks. 1860-1865. Montreal, 1865, pp. 426. (Of this volume p oh
1-24 were issued in November, 1861 ; pp. 25-56 issued January, 1862; pp. 57-168 issued June, 1362; pp.
169-344 issued February, 1865; pp. 395-416 prea. in Canadian Naturalist, vol. 5, 1860, pp. is
a

SM CCAa PAST r AR tars Voie Ge tate RCE
RSS SRE as see J Renae sae Fos 2
: e ; |. guage eeieiaieiiemmae Re ee

species, Arohapcyathus profundus ; and in the same year dasdeibed
cro rtreta gemma from near Portland Creek.
he mode of occurrence of the Cambrian section and fauna on the
shwest coast of Newfoundland is given by Sir William Logan in the
iption of the geological section near Bonne Bay.!
‘om a collection of fossils from Newfoundland sent by Mr. Alexan-
Murray to Mr. BE. Billings, there was described in 1865 Bathyurus
arius=Solenoplewra gregarius from the Paradoxides horizon of south-
st Newfoundland.? Subsequently he *described the fauna found at
at Bell Island and also “ Fossils from the Menevian Group,” under
ch we find Qbolella? miser, Straparollina remota, Hyolithes excel-
, Agraulos socialis, A. strenuus, A.affinis, Solenopleura communis, Ano-
nus venustus, Paradoxides tenellus, P. decorus, Iphidea, n.gen., Iphidea
ella, Stenotheca pauper, Scenella, n. gen., Scenella reticulata. Also from
tl he shales and sandstones of Great Bell Island, Conception Bay : Hophy-
ton linnecanun, Hi. jukesi, Arthraria antiquata, Lingula murrayi, Lin-
gulella (?) affinis, L. (2) spissa, and Cruziana similis. -
. With the exception of Obolella ? miser, Solenopleu ra communis, Steno
cou pauper, and Scenella reticulata the species described in 1872 were
: ublished i in the appendix to the report of progress of the Geological

ar urvey of Newfoundland for 1881.

In 1878 Mr. J. F. Whiteaves described‘ a new species of Lingula, Z.
iu ingsiana, from the shales of Kelley’s Island, and republished Mur-
"a uy’s geological ; section on Manuel’s Brook, sSudtionat Newfoundland,
vi ha list of fossils collected there as Balioiya: : 1. Agnostus acacia
, Agnostus (sp. undet.); 3. Microdiscus punctatus ; 4. M. dawsoni; 5.
mocephalites tener; 6. OC. baileyi; 7. CO. orestes?; 8. Paradowides
indet.), stating rae Nos. 1, 3, 4, 5, 6, and Gesuibty 7, are common to
P rimordial slates of St. J Phi, New Beieawiok: and to the shales of
Mi mnel’s Brook.

In 1887 when reviewing the Cambrian faunas of Cape Breton and
ffoundland Mr. G. F. Matthew® described a new species from the
nellus zone, Solenopleura bombifrons, and identified from Manuel’s
ok Paradoxides sp., Agnostus gibbus (?), Agraulos socialis, and Hy-
les essp. From Trinity Bay he identified in addition to the species
tioned by Mr. Billings Hocystites SP-, Agnostus levigatus, A. punctu-

Jogical Survey of Canada; report of progress from its commencement to 1863. Montreal, 1863.

oz0ic Fossils, vol. 1. Containing descriptions and figures of new or little known species of
remains from the Silurian rocks. 1860-1865, p. 363.

ome fossils from the Primordial rocks of Newfoundland. Canadian Naturalist, new ser., vol.
‘pp. 465-479.

ome Primordial fossils from southeastern Newfoundland. Am. Jour. Sci., 3d ser., seb 16, 1878,

€ Cambrian faunas of Cape Breton and Sewfoundland. Roy. Soc. Canada Proc. and Trans.,
4.1887, ‘PP. 147-157,

8 Oe SORA mtg eae ae tad Mere ees on Soe Sega ee aes
ner a oF ay By, POM > retes ie
‘ - be we mage ee
Se ‘THE CAMBRIAN. or VP i eS ee
a ee ae at

Osus, var., i inetd of three other species, and ‘Micvadionan: ‘tolls tus,

_ From Highland Cove in the same bay, Paradovides davidis, Centro.
pleura loveni, Agnostus punctuosus, var., A. brevifrons, A, levigatus, Ag a
Sree, var. declivis. es
~ In connection with the study of the stratigraphy of the Gambeinnll
rocks of Newfoundland, the writer described’ a number of species from —

_ the lower or Olenellus zone, and the middle or Paradoxides zone, 4
From the former there were Obolella atlantica, Coleoloides, n. gen.) —
Coleoloides typicalis, Hyolithes terranovicus, H. similis, Helenia, n. gen., —
Helenia bella, Microdiscus helena, Olenellus (M.) broggeri, Avalonia, n.. 4
gen., Avalonia manuelensis, Solenopleura harveyi and S.howleyt. From —
the Paradoxides. zone there was described the genus Karlia and the —
species K. minor.? .
In 1890 Mr. ©. D. Walcott? described Agraulos strenuus, var. asutus, .

from Manuel’s Brook. cd > | a

ge
“a
+s

NEW BRUNSWICK AND CAPE BRETON, 3 ai

s a <a
”

The first description of the Cambrian fauna as found at St. John, —
New Brunswick, by Mr. C. Fred. Hartt‘ included the following species ; d
Eocystites primevus Billings, Lingula matthewi, Lingula, n. s., Obolella —
transversa, Discina acadica, Orthis billingsi, Orthis, n. sp., Conocephatites 4
baileyi, CO. matthewi, OC. robbi, C. orestes, C. elegans, C. owangondianus, OF%
tener, C. aurora, C. thersites, C. gemini-spinosus, C. halli, C. quadratus, OC. a
~~ neglectus, C. ae Conocephalites, n. sp. (?), Microdiscus dawsoni,

: -Agnostus acadicus, Agnostus similis, Paradoxides lamellatus. A
It appears that the Hocystites primevus wassubmitted to Mr. Billings, ©

to name the genus and species, in manuscript, and was printed i in con- — |
nection with Mr. Hartt’s paper. The Paradowxides micmace, figured by |

Dr. Dawson at the close of Mr. Hartt’s paper, was named by the latter —

in manuscript. The figure is a restoration, and no description accom-
panies it. In the report of Messrs. Bailey and Matthew? it is stated —
that Mr. E. Billings identified from the St. John group, in the Kenne. |

- beeasis Valley, fragments of Paradoxides and the pygidium of an
Agnostus, three species of Conocephalites, one of Ellipsoeephalus, one
of Agnostus, what appeared to be a fragment of Salterella, and speci-_
mens of Palzophycus of two or three kinds. Among the collections —

examined by Prof. J. F. Whiteaves for Professor Bailey® there is anew —
a “a
1Descriptive notes of new genera and species from the Lower Cambrian or Olenellus zone of North
» America. U.S. Nat. Mus., Proc., vol. 12, 1889, pp. 33-46. st
: 2Descriptions of new genera and species of fossils from the Middle Cambrian. U.S. Nat. Mus.
Proc., vol. 11, 1889, pp. 441-446.
3 The fauna of the Lower Cambrian or Olenellus zone. 10th Ann. Rept. U.S. Geol. Sur., 1890, p. 654.
4¥Fossils of the Primordial or Acadian group at St.John. Dawson, Acadian Geology, 1868, pp. 641— q

-

j
|

657. =e
= 5Preliminary report on the geology of southern New Brunswick. Geol. Surv. Canad., aes. Prog,
: 1870-1871, 1872, p. 140. a

6 Report on the pre- -Silurian (Huronian) and Cambrian or Primordial Silurian Rocks of Souther ma
New Brunswick. Gcol. Surv. Can. Rep. of Prog., 1877-78, 1879, pp. 30, 31 DD.. x te Se

rss ERAGE ER AT Ges ren NY tage mn See A Po CNS
ihe mone. rick ae 2 3 Ks
" PALEONTOLOGY—NEW BRUNSWICK. 81

2 of the St, ibn group made its me RS In this is given a
f historical review of the work that had already been done upon
he fe fauna by Prof. Hartt, and a statement that from the collections made
rom 1 time to time during the progress of the Canadian geological sur-

Bains and Salterella and the eS of two species of Hyolithes.
des these, there are the supposed plant remains of the genera Pale-
mene, Eophyton, etc., of the higher divisions of the St. John
ZrO ap.” Mr. Matthew made large collections, which were destroyed by
he great fire at St. John iu the spring of 1877. His published studies
based upon new material collected subsequently to that date.
the first memoir we find that he recognized three well defined spe-
of Paradoxides and six varieties, as follows : Paradoxides lamellatus
ts P. lamellatus var. loricatus Matthew; P. acadicus Matthew; P.
ninicus Matthew; P. eteminicus, vars. Bainaiden, breviatus, quacoensts,
icitus, and eh acalic

A review by Mr. C. D. Walcott? of the typical collections upon which
of _C. F. Hartt based his species, led to a revision of the genera and
pe ies, with the following results :

- Lingula matthewi....-.--. = Acrothele matthewi.

Discina acadica........-.. = Paleacmea (?) acadica.

_ Theca acadica ..--...- .--.= Hyolithes acadica. Sy

_ Agnostus similis .........= Agnostus acadicus.

-: Microdiscus pulchellus...—= Microdiscus punctatus Selter.
~ Conocephalites matthewi — Conocoryphe matthewi.

gemini-spinosus -... - = Conocoryphe matthewi.
_ baileyi ..:.-.....-....= Conocoryphe baileyi.
pr QPOGANS). 2 5162 <2 -s5- = Conocoryphe elegans,
PRR ed cree SEES te Ss Shes = Ptychoparia robbi.
-formosus...-... Coe OE = robbi.
ouangondianus ...... = ouangondiana.
BMI Ds i etn eens eS. = ouangondiana var. aurora.
Siuedrata: 22.2.2... as quadrata.
orestes..... See oe orestes.
Raeee Ghersites ..2-..2< .5.. - = _ orestes var. thersites.
aeney s.-.. 2. ee at. 2S tener.
=a gre Beeman it, eae tener.

elloid form of Sioone Mr. Matthew was ea to give
tO ethe new species, other than the preceding, and he proposed
Saal (p. 15), Hyolithes danianus (p. 20.), Hyvlithes miemac

108. Snpplementary Abition: oa 271-279.

p.8

an faunas of North America; jesitiainary studies. U.S. Geol. Surv. Bull., No. 10,

N

~

ry ini, =) 63 eel tah ee. <a Os Cars lcs fee Sabato we
'? ‘ af o >t =) ' Siig > x x itr, a ae ‘ 2 a wae aS -
‘i 4 mae ; ‘ 4 tl ; ve Re eae . Fina Bb tee 5 ee
Shor Se ss Ey cA ath. 5), Ste a ep a eer t s.:
‘ S55 “ ae oe , See 1m 3 c So
BB. ore “THE CAMBRIAN, a ay ea Sy :

| _ papers read before the British Association for the Advancement of ‘ci i-

He sent them to Prof. Hyatt, who wrote that the aspect of the sipho

(p. 21), Conocoryphe walootti (p. 30). The sirtspsttons Salteria was | Dro:
posed by the author to include the Conocephalites baileyi of Hartt. —

All of the species were figured and described, with the exoaphion dy of
Conoco ‘yphe walcotti. This included figures of the three species OF f
Paradoxides, P. lamellatus Hartt, P. acadicus Matthew, and P. eteminicus
Matthew. =

Some of the results of Mr. G. F. “Matthew's studies are given in two
ence at the Montreal meeting in 1884. In one he refers to the geolog-
ical age of the Acadian fauna, and correlates it with the fauna of 16
St. John group and that of the Solva group of Wales. In the secon d
is given a description of the development of Ctenocephalus matthewi anc id
other species of the genus Conocoryphe.? , 3 am

In Mr. Matthew’s second memoir on the fauna of the St. J ohn group; 3
presented to the Royal Society of Canada in 1884, additional notes 4
given of the Paradowides acadicus and P. lamellatus. He hope he
name Paradoxides micmac for a large species, which he thinks is: prob. 0)
ably the one figured in Acadian Geology. The original species te
which Mr. Hartt intended to apply the name is unknown. The Con 0
cephalites matthewi of Hartt is referred to the genus Orenocspneaaa
Corda. <A detailed description is given of the species, and also of t
various stages of its growth, as found in the St. John slates. Conocory
phe baileyi, C. elegans, and CO. walcotti are described and figured. In: a
description of the plate® the subgeneric name Hartella i is placed afte
Ctenocephalus and Bailiella after Conocoryphe. |

In 1885 Obolella transversa Hartt was referred by Mr. C. D. Walec 9)
to the new genus Linnarssonia, together with the closely allied Mer
vian species, Obolella sagittalis. ® | a

In a paper read before the Natural History Society of hadi Bran
wick in 1885, Mr. G. F. Matthew stated’ he had found some Pteropod
that appeared to have several distinct septa at the base of the tu ‘

|

is due to the compression of the sharper against the flatter side. Th 3
form of the sutures favors this impression. ‘These fossils with the
distinct septa are startlingly similar to certain forms of Nautiloideé
but there is no siphon. They, however, confirm Von J hernig’s and m
opinion that the Orthoceratites and Pteropods have had a comnonal
as yet undiscovered, ancestor in ancient times.” ie

*

xs
us

1 Op. cit., pp. 31, 32. =
2The geological age of the Acadian fauna. The primitive Conocoryphean. British Associati
Rep., 54th mecting, 1834, pp. 742-748. The geologic age of Acadian fauna. Geol. Mag., new ser., dee
3, vol. 1, 1884, pp. 470-471.
' 3]Ilustrations of the fauna of the St. John group, continued; on the Conocoryphea, with furthe
marks on Paradoxides. Royal Soc. Canada, Trans. and Proc., vol. 2, sec. 4, 1885, pp. befits # a
4Qp. cit., p. 101. 5 Op. cit., p. 124. ; . Bots
6Paleontologic Notes. Am. Jour. Sci., 3d ser., vol. 29, 1885, p. 115. Ty

_7An outline of recent discoveries in the St.Johngroup. New Brunswick Nat. Hist. Soc. Ball.,N Oo.

- ° Saree eS ‘ee Fe a N ee hl ee i) Se _ FO ot OOGN eer ©. oN
ST Sa shia od Chae eo oe Ae ft x SRS PARNER tS, . :
PA, *

ae the Patios, Archeoe yathus ? pavonoides, Pestiiponsiik minor,
a .? minor, var. distans, the new genus EKocoryne and the species “Bobo.
ve geminum are described. Of Hydrozoa Dendrograpsus ? primordialis
_Protograpsus, n. g., with the species Protograpsus alatus. But one spe-
nga the Echinodermata is mentioned, Hocystites primevus of Billings.
‘he new forms of Brachiopoda are: Tague ? inflata, L. linguloides,
otreta baileyi, A.? gulielmi, Kutorgina latouwrensis, K.? pterineoides,
Orthis quacoensis. Of species previously described Lingulella dawsoni,
Linnarssonia transversa Hartt, Linnarssonia misera Billings, Acrothele
matthewi Hartt, and Orthis billingst Hartt, are described and illustrated.
~~ Among the Pteropods the new subgenus Camerotheca is proposed,
an d phe species Hyolithes caplet eae gr eee “Ee) danianus, and

, a .
Ms ¢ ‘gk

© Fa

“teadicns sof Hartt, isd its Sepecabics sericed, yi eiek atl Crassa.
The Gasteropoda include « notice of the genus Stenotheca and the )
description of the new species, Stenotheca hicksiana, S. concentrica, S. ra-
diata, S. nasuta, and 8S. triangularis. The subgenus Parmophorella is
Bs posed to include the original species, Discina acadica Hartt. Steno-
a Bion 1 acadica and Harttia matthewi Walcott are described and illus-
| as To the Phyllopoda (?) the new genus Lepiditta, with the species
alata and L. curta, and the new genus Lepidilla, with the species
| dilla anomala, are referred. . Matthew says that these forms
very minute, and belong either %6 lamellibranchs or Phyllopods.
e Ostracod Crustaceans include the new genera Hipponicharion and
richona. One species is referred to the former genus, H. eos, and
» to the latter, B. papilio and B. tinea. To the genus Primites he
$s one new species, P. acadica.

ie Trilobita include the new species of Agnostus, A. regulus, A.
rtitus, A. vir, A. vir. var. concinus, A. tessella, A. umbo, A. obtusilobus,
A. acutilobus. Agnostus acadicus Hartt is described and figured and
5 variety declivis proposed. Microdiscus pulchella Hartt is placed as
ariety of M. punctatus Salter, and a new variety, precursor, is pro-|
sec ae be included under pees. M. dawsoni Hartt is also descr ibed

: a for the first time, and Pa ndddnites dealt is proposed as a
pecies. A ee of Seats opie micmae and the proposal

rat ons of the fauna of the St.John group, continued. No. IIT. Descriptions of new genera
ies (including a deseription of a new species of Solenopleura by J. F, Whiteaves). Royal Soe.
1 rans. vol. 3, sec. 4, 1886, pp. 20-84. (Proce. for 1885.) -

. Eo PALEONTOLOGY—NEW BRUNSWICK. - aE a ee

“ah Ye ee 5 ee ee ee ee em See aed rea = ae
Sey ape ret or P aaaa ete Wide nen chee 8
a i ose 4 Sool ye if: 4 eo ‘ * = 2k x4 ~
+e poe = S-Z ~ a SAT ee pd
“te ‘ | As “ee i
84 - THE CAMBRIAN. Ze at es s ae
= mm es Saas

twenty-one varieties of fossils.

species :?

Anopolinus? sp.
Parobolina? sp.
Anomocare? 2 sp.

- Ptychoparia, 2 sp.
Agraulos socialis Bill., var.
Microdiscus punctatus Salter, var.?
Agnostus acutilobus (cfr. gibbus).

In some preliminary notes on the higher fauna’ he says that—

The heavy band of black slates which runs through the center of the city of Saint,
John has yielded the following species, contained in calcareous nodules :

Ctenopyge (efr.) spectabilis Brégg.
Orthis (cfr.) lenticularis Dal.

These indicate a horizon in the upper part of the Lingula flags. Ki
A series of slates are exposed along the north side of the Kennebecasis Basin, whoa
fossils indicate that they also pertain to the upper part of the Cambrian Systane

Conocephalites, aspecies with broad

free cheek and flaring genal_

spine,
Ptychoparia, a small species.
Agnostus (efr.) pisiformis Ang.
A. (cfr.) richmondensis Wal.

Ina synopsis of the fanhé | in ‘OT ision 1 of the St. John. group, } Mr.
Matthew! notes the occurrence of thirty genera, sixty- five species, an a
He states that in a higher horizon i
the Kennebecasis Bay area he has found the following association ¢ of i

Arthrari ia, Sp.

Agnostus (ofr. Nathorsti, Brégg

A. (cfr. parvifrons, Lins.) :

A. umbo. .

A. acadicus Hartt, var.

Hyolithes, sp.

Linnarssonia transversa Hartt, sp.

Kutorgina (cfr.) cingulata Bill. —
Kutorgina ?

Kutorgina (?), sp. .
Lingulella (cfr.) lepis Salter, —
Lingulella, sp. es | :

- Eophyton linnzeanum Torrell, var, 2

Eophytera, sp.

In a note to the American Journal of Science Mr. Matthew 4 state Ss
that he has found Olenellus (?) kjerulfi in the Kennebecasis River:
_ Basin in band ¢ and d of his Division 1; and that the same species —_ .
in the Cambrian beds of N ewibaidland: Upon this reported discovery
Mr. S. W. Ford® endeavored to show that as the species was found a
the base of the St. John Paradoxides beds and at the base of the Swed-
ish Paradoxides beds it was a true Paradoxides, and therefore did ne rt
influence the question of the stratigraphical paged of the Oleneltus,
fauna in North America.

In an abstract of a paper on the Cambrian yea of F Cape Breton < ant qd
Newfoundland in the Canadian Record of Science, vol. 2, 1886, pp. 25
258, that preceded the main report in the Royal Sécléty of Canada,
Transactions,° Mr. G. F. Matthew points out that the slates of Mira’
River, Cape Breton, contain several species of trilobites, which show
that these measures are in the upper part of the Olenus zone or Lin igula-
flags of Great Britain. The species observed were Peltura scarabeoide 5

4 ‘a

“1sy nopsis of the fauna in Division 1 of the St. John group, with preliminary notes on ‘the higher
“faunas of the same group. New Brunswick Nat. Hist. Soc., Bull. 5, 1886, pp. esl, aS

2 Op. cit., p. 29. 3Op. cit., p. 30. ‘ c la

4Note on the occurrence of Olenellus (?) kjer uli in America. Am. Jour. Sci., 3d ser., vol. 31, 1886, p. 4 72.

5 Note on the age of the Swedish Paradoxides beds. Am. Jour. Sci., 3d ser., vol. 32, 1886, pp. he

6 On the Cambrian faunas of Cape Breton and Newfoundland. Royal Soe. Canada, Fi Proc. and Tra
vol. 4, Sec. 4, 1887, pp. 147-157, ;

: Pe ee _ PALEONTOLOGY —NEW ‘BRUNSWICK. 85

ot the St. John eroup, and an Orthis similar to Orthis inde
of Dalman.

In n discussing beieidonde afforded by the smaller-eyed trilobites of
| vision 1 of the St. John group, Mr, G. fF’. Matthew! speaks of their
ing on the origin of the Cambrian fauna. He also gives a list of

on known to him at that 3 from eee 1 of the St. John series.

x of the St. oka group.2- Meztion i is diusiig by Mr. Matthew of ad.
nal species from the St. John group in 1888.3 In the measures on

h St. John Basin, a calcareous organism that may be referred to Old-
vamia v has been febnd- It resembles O. antiqua, but branches less freely.
n th he Same sandstone occurs an elegantly ornamented Linguiella (?) of

rT: Balter form. Mr. Matthew compares it with Lingula ? favosa of the

nyton sandstones of Sweden. In Division 2 of the St. John group

s related to Taonurus or Spirophyton; also fragments of bodies
yt small crustacean that is probably a Ilymenocaris. In a paper pub-
| ishe soon after. on the “Classification of the Cambrian Rocks of Aca-

ia, ” Mr. Matthews states‘ that the Lower Potsdam of Billings, or
Begish n of Mr. Walcott, is found in the island of Cape Breton, where

ps. Remarks upon the affinities of the characteristic genera of
RN,
et and other portions of the Cambrian fauna_occur in this

: aS species is referred to the genus tillipeocephavas se
ul Los? whitfieldianus is described with its variety compressa. The
US ‘Strenuella is proposed, with the species Strenuella ? halliana
type. A discussion of the genus Liostracus of Angelin is

Pec

>a varieties immarginata, aurora, gibba, and plana, and a

| (Paradoxides: regina). Part 2: The sraallér trilobites with eyes Bes daied ie and Ellip-

4 al Soc. Canada Trans., vol. 5, sec. 4, 1888, pp. 115-166.

ons of the fauna of the St. John Group. Canadian Ree. Sci. vol 2, 1887, p. 361. “5

series of Cambrian rocks in Acadia. Canadian Record Science, vol, 3, 1888, pp. 28, 29.

Ree. Sci., vol. 3, 1888, p. 74.

tions of the fauna of the St. John group, No. IV. Pt. 1. Description of a new species of
*2 > arene regina). Pt. 2. ites smaller trilobites with eyes (Ptychoparide and Ellipso-

St. John River corresponding to those of Band B in Division 1 of -

peu several genera of seaweeds, among which are two graceful

ssils are Bathyurus (sub-genus?), Orthisina, Orthis, and i yolithes —

d by descriptions of Liostracus tener Hartt, L. ouangondianus.

Pia ee BONS SESS ARTE Siege PRS RETO) ha oe Se
> : ss y eal Won Race Ps OS peed
Z ee OE hs Uae: SS rie eageeien
5 Le Ps BOE Sn? RSS Pee Se hen en
. F > . es 2K \ we . By ee \ ts aoe Be a og .
a ‘ sii ag! as £4 b ; is A re ow
86 % THE CAMBRIAN. ret ea ee etext 4

~

-. the genus Solenopleura of Angelin he refers the Conocephalites robbi of

:

_ Series B. In all the fine layers of this band species cf Protospongida 7

_ found to be a narrow, and P. micmac a broad form of Paradowides hickst —
_ of Wales (p. 385). From stage 2, the Olenus beds, he reports abun- —

‘notice of the development of the young of this species. Under Pty. e
choparia, Liostracus linnarssoni Brégger is identified from the St. ‘_
John series. Tor the narrow form he proposes the variety alata, and
this is followed by a description of the development of the young. Tord

‘Hartt, and gives a description of the development of the young as far —
as mci to him. A more extended description of Solenopleura acadica —
of Whiteaves is given, and the variety elongata proposed. -.
In the second paper by Mr. Matthews on the classification of the —
Cambrian rocks in Acadia! the species Obolus pulcher is_ dascribed’™ .
from the base of Band B of division 1 of the St. John group. In the —
middle of the band Mr. Matthews recognized an Agraulos and at the —
base an Ellipsocephalus. This paper also contains a discussion of the —
—Olenellus fauna as found in Nevada. In a paper read later in 1889,
entitled ‘* On the Cambrian Organisms in Acadia,” Mr. Matthew States _
that he has found in this lower series beneath the Paridoxides zonea —
species, that recalls Pucoides circinnatus (p. 384), the Obolus which was _ |
described later, and undoubted examples of Platysolenites of Pander. —
In mentioning the fauna and flora of the Paradoxides beds, he says the
basket sponges and the rod like sponges (?) are common to both this and |

may be found, but no examples of the typical Protospongia of the Par- 1
adoxides beds have been observed. A new species of Obolus and three
species of Lingulella are mentioned as being described in the paper, and
the Algze are represented by several different types, among which are
a Buthotrephis and a microscopic form parasitic on the latter organism. —
There are also’some quite small oval forms, resembling Hydroeystium, —
which may have been algoid. Among the new species of the Paradox-
ides beds is a little Platyceras. He says that Paradoxides pontificalis is 4

‘dant remains of a large Protospongia, including Protospongia fenestrata —
of Salter, and P. (?) major of Hicks, and another large species. From

- the fossils which appear to have been placed in the upper part of divi-

sion 2 are some that have been found in Kennebecasis Basin of the
Cambrian rocks. These are Leptoplasti, allied to LZ. stenotus of Ang: | .
-elin, Agnostus pisiformis, var. and Agnostus nathorsti, var. From —
division or stage 3, the Peltura beds, he mentions two species, Cteno-
pyge (ef. C. Aagillifer and (C. spectabilis), Orthis lenticularis, and a Ku- |
torgina. At the bottom of the division Lingulella lepis and another
large species, L. ampla, var.? are found. These beds are correlated with |
beds of Cape Breton containing species of Peltura, etc. (p. 386). a

th a paper by Mr. Matthew, entitled ‘* How is the Cambrian divided t

1Canadian Record Science, vol. 3, 1869, pp. 303-315. ? Ibid. , Pp. 383-387. 4 -
; .

si ae ie " PALRONTOLOGY—NEW BRUNSWICK. Bicone
: wa £m, is ae -)) aa : ”

Lp lea i or the classification of Salter and Hicks,”! a comparison of the
en enera of the different horizons of the Cambrian is made. ie

£: n the full paper on the Cambrian organisms of Acadia, published in
890, Mr. Matthew describes the stratigraphic position of the fauna that
peowelelees beneath the Paradoxides beds, and compares it with the
> Cambrian fauna of Sweden and Russia. The new genera and

ee x ies described are :?

4 _ Phycoidella, n. g.,p. 144. _
.. ; & _ Phycoidella stichidifera n. sp., p. 144,
-Paleochorda setacea n. sp., p. 145. ;
* Hydrocytium (?) silicula n.sp., p. 146.
ae Microphycus n. g., p. 146.

_ Microphycus catenatus n. sp., p. 146.
_ Monaditesn.g.,p.147.

ate Monadites globulosus n. sp., p. 147.
- Monadites pyriformis n, sp., p. 147.

a -Monadites urceiformis n. sp., p. 147.

- Radiolarites n. g., p. 148.

IS - Radiolarites ovalis n. sp., p. 148.
} ao. _ Plocoseyphia (?) perantiqua n. sp., p. 148,
; Astrocladia (?) elongata n. sp., p. 148.
Bey Astrocladia (?) elegans n. sp., p. 149. eas
= - -Astrocladia (?) virguloides n. sp., p. 149, :
Bae 3 Dichoplectella n. g., p. 149. "
a oh _Dichoplectella irregularis n. sp., p. 149.
_ Hyalostelia minima n. sp., p. 150.-
S Oholus (?) major n. sp., p. 155.
Lingulella martinensis n. sp., p. 155.
. _ Leperditia ventricosa n. sp., p. 159.
Be set - Leperditia steadi n. sp., p. 160.

: Q Iso describes and illustrates :-

F ee omerh antiqua Brongn., p. 144,
Platysolenites antiquissimus ichw. .» p. 150,

Obolus pulcher Matth., p. 151. :
Voters tenuis Schmidt, p. 156. ,

_ Psammichnites gigas Torrell, p. 157.

s-

-. Sea lyelli Torrell, var. minor, p. 159.

t with acceptance from a number of naturalists and the generic

ns of the genera) Olenellus, Olenoides, and Mesonacis.

a ‘note at the close of the descriptions it is stated that he haa .
that a suggestion made by him in reference to Olenellus kjerul fi.

olmia i is proposed for Olenellus kjerulfi.2 Mention is made of the

Ne RAS aS ges Sue ae ee a es a sat Ae i a Sto %
Drea ett ONG Scope Leb Fb Bat te Se to
Oe Rete ee EE we Uy pea pet Ree i al aN
> <% i, ig As Pe eee ray ba: >
: 83 Dia se THE CAMBRIAN. zn Sees Sect Pies >
—s. a > =s!
cate ers . ; Se ea

-lella starri, 0 . 8D., p. 146, “Lingulella ae n. sp., Dp. 147, Boichnites,
> ay Ben., “pi 148,- Otenichnites, n. gen;, p. 15 Ctenichnites ingens, nD. SP.
- -p. 151, Frena ramosa, n. sp., p. 159, Lvenbeiiiies brevis, n. Sp., ip 159,
+ Gouiadicnwites. n. gen., p. 160, Goniadichnites trichiformis, Nn. Sp. e 169, a

_Monocraterion magnificum, n. sp., p. 161. -¥
In addition to the preceding Mr. Matthew has remarked upon several
_ genera and species that have been previously described from the Cam-
brian rocks. They include: Hocoryne geminum Matt., p. 130, lent =
— anomala, Matt., p. 130, Orthis and Orthisina, p. 131, Aisaathaes Salter, p. —
132, Stenotheca concentrica, Matt., p. 133, var. radiata Matt., p. 133, —
Bicasiheon triangularis Matt., p. 134, In his remarks upon the genus :
Stenotheca he concludes that the type species is not a mollusean shell, 4
but should be referred to a Phyllopod crustacean. This includes thei”
typical form, but does not include Discina acadica, of Hartt, as the latter | “
is a patelloid gasteropod. Conocoryphe waleotti Matt., p. 134, Concory-
phe baileyi Hartt, p. 135, Paradovides lamellatus Hartt, p. 135, Paradox-
ides micmac, var., pontificalis Matt., p. 136, Agraulos (?) whitfieldianus: i
Matt., p. 188, Agraulos socialis Bill., p. 188, Medusteas princeps Torrell, Pe
140, Medusites radiata Nathorst, p. 141, Medusites costata, p. 142, ‘eich a
nites linneanus Torrell, p. 148, Pulirknibanes Torrell, p. 157, Frena, :
Roualt, p. 168, Monocraterion Porrell v. 160, Monocrateriéh tentaculatun,
No “p. 161, Histiollerma hibernicum, p. 162.
s

er EASTERN MASSACHUSETTS. : y
The first description of a fossil from the Cambrian rocks of oasteeaen

“Massachusetts is that of Paradoxides harlani, by Dr. Jacob Green,! from
specimens sent to him by Dr. Richard Harlan, who supposed they came —
from Trenton Falls, in the State of New York. It was not until 1856? — 4
23 that the true horizov from which the specimens came was discovered. _
In making the announcement of the discovery Prof. Rogers quoted

from Barrande on the distribution of the genus Paradoxides, and stated

- . that he considered the specimens from Braintree, 10 miles south of —
- Boston, to be identical with the Paradoxides harlani described by Green |
jn 1834. He says the fossils in the Braintree quarry are in the form of —
casts, some of them of great size and lying in various levels in the
strata, and that as far as he could observe they all belong to one spe- —
cies and agree more closely with Barrande’s Paradovides spinosus than Be
oe with any other form known to him. A fine figure of Paradoxides har-
Bo. fant was published by Prof. Rogers,’ in his final report of the ceolopionls
survey of Pennsylvania, under the name of P. spinosus. |

Mons. J. Barrande, in referring to the discovery of Paradoxides in

the slates of Braintree,‘ institutes a comparison of the Specimens from

- Descriptions of some new North American trilobites. Am. Jour. Sci., vol. 25, 1834, p. 336. ‘

2Proofs of the Protozoic age of some of the altered rocks of eastern Massachusetts, from fossils

oS - recently discovered. Am. Acad. Proc., vol. 3, 1856, pp, 315-318. e 4 ae
oo ee 3’ The Geology of Pennsylvania, Philadelphia, 1858, vol.2,p.816. = Wy
‘Trilobiten der Primordial-fauna in Massschnsotia. Neues Jahrb. for 1860, pp. 429-431. ee te a ‘

-
-

- Sr f = ™~

“PALEONTOLOGY—EasTERN MASSACHUSETTS. — 89.

,

mn d Paradowidés spinosus from Bohemia, and concludes that ef
| n Pp esuony i. for P. spinosus. —

_ In 1861 Prof. Jackson! exhibited a small trilobite from Braintree of
the species Paradowides harlani, stating that it seemed identical with
r s from Newfoundland described as Paradoxides bennetti f from 8 St.

la ry’s tach Ina a foot- note accompanying a “paper on the geology of

a
f Sailings informs me that he regards the Paradoxides bennettii (Salter) from
Vv foundland as identical with the Par adoxides harlani (Green) from Braintree. ~

\ number of collectors obtained specimens of Paradowides harlani
| from Braintree beds, but it was not gee 1861 that a notice of other

fis which is referred to the cenus Ellipsocephalus. He also reported
ding a distinct fucoidal impression which shows three branches, each
abot ; 4 inches long, but not sufficiently well marked to afford any evi-
der ce. as to its nature. Mr. Ordway also published a figure of a head
of Paradovides harlani when comparing that species with Paradoxides-
8) nosus, Boeck., considered by Barrande identical with P. harlanis
In his notes on the geology of eastern Massachusetts Mr. W. W,
: De dge® reviews the then existing information in relation to the fauna.
oO! the Paradoxides zone of Braintree—the Braintree slates— mentioning
radoxides harlani and a few obscure traces of fossils found at that lo.
1 iy: A general description of the Cambrian fauna of Wales is given
in th a connection.
Mie second described species from the Paradoxides beds of Braintree
s Ar ionellus quadrangularis by Prof. R. P. Whitfield.6 This is probably
she species of Ellipsocephalus referred to by Mr. Ordway.
A review of the fauna of the Braintree argillites by Mr. ©. D. Wal-
‘included a mention of the species previously described, and a de-
* ion of a new Pteropod, Hyolithes shalert, and a new species of
ite, Ptychoparia rogersi. The species described by Prof. Whit-
is Arionellus quadrangularis was referred to the genus Agraulos.
ler the title of “ Preliminary descriptions of North Attleborough
y? ” Messrs. N. S. Shaler and A. F. Foerste* made the most impor-
tat co ntribution to the Cambrian fauna of Massachusetts since the
ISCO' By of Paradoxides harlani. They identified the fauna as that

he alia of pier foagit Saris at Brdiateed Mass. Boston Soc. Nat. Hist. Proc., vol. 8,

on the geology of eastern Massachusetts. Boston Soe. Nat. Hist. Proc., vol. 17, 1875, pp.

oe of some new species of Primordial fossils in the collections of the Museum, and correction
svi sly described species. Am. Mus. Nat. Hist., Bull., vol. 1,1884, p. 147.

‘Cambrian ‘Faunas of North America; prelitainaty ptadies, U.S. Geol. Surv. Bull. No. 10,
pp. 323-329. Separately paged, pp. 43-49.

Maus. Comp. Zool., Harv. College, vol. 16, 1888, pp. 27-39.

. eally, if not specifically, vere sal. This removes Paradoxides from the

* close affinities with the Braintree Cambrian horizon. He made careful |

—_

a pene: HP S Ret Ban Farsi ek Poe PRS eRe pee
ote s a ates A ee Wate ee Fee tgaice RL eR a4
nei elan a ie ciety Bere et ee So iit: 3 ets ee
SOGRS rere ay THE CAMBRIAN. gh ae ones
of the Olenellus ZONe, as s found 4 in the vicinity of Troy, Wer: York. ‘The os
neers described are: 3 A , “ae
Obolella crassa, var. H. communis var. emmonsi. . _
~ Obolella (?) H. americanus. | | . 6 Se
Fordilla troyensis. H. princeps. , a
Lamellibranch (?) H. billingsi. —
: Scenella reticulata. Hyolithellus micans, m _"
~ Stenotheca rugosa, var. paupera. Salterella curvatus, | 7
_§. rugosa var. abrupta. ~ Aristozoé. .
S. curvirostra. _ Microdiocus bellimarginatus,
Platyceras primevum. M. lobatus.
Pleurotomaria (Raphistoma) attle- | Paradoxides walcotti.
borensis. Ptychoparia mucronatus.

~~

~

- ju

x

genera and four species, and from the Olenellus or Lower Cambrian |

-10n the geology of the Cambrian district of Bristol County, Massachusetts. Ball. Mus. Coes ZoOln,

Hyolithes quadricostatus. — .

Of these, two genera—Pleurotomaria and Paradoxides—have. not
heretofore been found in a strongly marked Olenellus zone fauna. A 4
comparison of Paradoxides walcottt with specimens of Olenellus asa—
phoides from Troy, New York, of the same size, show them to be generi- 3

Ptychoparia attleborensis. _

_Olenellus fauna. .

Under the view that the Olenellus fauna preceded the Paradoxides *
fauna Prof. Shaler! speaks of Paradowides waleotti as the surviving
member of the series, and s say's the occurrence of the genus indicates :

search for indications of the stratigraphic relations of the North Attle-_ “4
- borough and Braintree section but without success. In mentioning the —
Braintree locality it is stated that a number of distinct remains occur —
near the Neponset River, and the beds have much the same aspect and —
are apparently about the same distance from the syenites as those at.
Braintree.” zs :
A notice and description of the fauna found at North Attleborough —
from the Olenellus horizon, was followed in 1889* by the announcement — a
of the discovery of Hyolithes in limestone near East Point, Nahant. &
Mr. Foerste correlates the limestone and associated shales with those —
of North Attleborough, and states that the species of Hyolithes appearg
to be the same as that found at North Attleborough. He proposes the ©
name of Hyolithes inequilateralis. From a study of the type specimens —
the writer believes it to be identical with H. communis var. emmonst. —
As now known, the entire Cambrian fauna from eastern Massachu- —
setts includes foie the Paradoxides or Middle Cambrian zone four |

zone, twelve genera and nineteen species. — : aan

Harv. College, vol. 16, 1888, p. 21. , y
2Op. cit., p. 23. : , *
3 Foerste, A. F. The paleontological horizon of the limestone at Nahant, Nah ndabeniitie Baten
Soc, Nat. Hist., Proc., vol. 24, 1889, pp. 261-263, wv

) a Wa i” > ae a, ; Maa, d 7 , : 7 a ; ,
ns Fl
<a 91
_

1 es Valley on the north, to Georgia and Alabama on the
h. 4
‘or the purpose. of erescniink the historical data the province will
ve di ivided as follows:
er A: Northern Appalachian district.
fis ie. ot Appalachian district.

fs
‘Ts

e* i MAS NORTHERN APPALACHIAN DISTRICT.

ie St. Lawrence River.

The Hudson River and Lake Champlain area will first be considered.
cludes the strata referred to the Cambrian, found on the western
of the Green Mountains, the foot hills and the more level country
hing westward toward the Hudson River and Lake Champlain.
earliest reference in the literature to a distinct formation that is
referred to the Cambrian is found in a description of the geology
estern Massachusetts and eastern New York. On this account this
mat ion, the “Granular Quartz,” will be treated historically as it
3 be en mentioned by authors in Massachusetts, New York, and Ver-
until the: year 1861, when its history will be carried few oud with
at of the “Red Handioek ” and the ‘Georgia Slates,” with which
18 then correlated. | .
ag ; x GRANULAR QUARTZ.

2

first differentiation of a formation referred to the Lower Cam.
2 America was made an Prof. Amos Baton in 1818, + Por to

é Paes and thence southwest throughout New Yor k, oe Jersey,
N vania, Virginia, eastern Tennessee, northern Georgia, and
lississippi. On the map accompanying a later work? the Transi-

C re son the dade of the ‘United States explanatory of a geologicalmap. Am. Phil. Soc.
1809, pp. 411-428, map.
s Nahas geology of the United States; with remarks on the probable effects that may
t he decomposition of the different classes of rocks on the nature and fertility of soils,
es “a Am. Phil, Soc. Trans., new BEF Volk 1, 1817, pp. 1-91.

a sk 3+

“_ ~ &
Be ks, See Ain +h
= en

oe ‘ tion rocks a are extended north into the valley 0 of

ented the * Gehiciss tickttons anid Quatte ” as s No. 5 of me }
_ tion, and an argillaceous and siliceous slate as No. 9, giving 1 the locali- -

ha hal

,
see
i ~

= oa ties. at which they occur. Two years later this classification was re-
“viewed? and the “ Granular Quartz” dropped out of the nomenclature,
We is only to reappear again with a very accurate description of the forma- s
oe ~ tion as it occurs in Vermont.‘ It is interesting to note in this ohne :
=i tion, that the “ Granular Limerock” is mentioned as accompanying the
es ; “ Transition Granular Quartz ” from Whitehall on Lake Champlain, to

£ rg tis a on the Hudson. Up to this time Prof. Baton appears to have a

_regarded the terms “ Granular Quartz” and the “« Granular Limerock se
z as sesh na eats. In the classification of 1824,° however, the “Gran: |
ular Quartz” is separated from the “ Granular Limerock ” and. fally “S
described. The “Transition Argillite” and the “ Primitive Argillite” 4 F
are also defined, and some of the localities given are now known es
localities of Lower Cambrian slates. The geologic profile accompany-
ing the memoir of 1824 exhibits the differentiation made by Prof. Eaton <A
: in the classification of the rocks by ee the primitive granite and WB a :
Se ~ secondary. |
: In the geologic nomenclature of to-day fis “Granular Quartz” is 4
-. jneluded in the Lower Cambrian, and the “ Granular Limerock” equals
tee the Trenton Chazy -Calciferous iieniass - The “ Primitive Argillites” re
of Williamstown Mountain equal the Upper Hudson or Lorraine | Be a
shales. The “Transition Argillite” is nearly all Cambrian, with ‘the —
exception of asmall portion near the Hudson River. The Calciferous. =
-_ gandrock is of the same age as the “Transition Argillite. 2 Re Gray- a Re: ;
—wacke of Peterborough Mountain, and the Metalliferous limeroek 858
of Silurian (Ordovician) age. The ‘Transition Argillite” is mostly
of Lower Cambrian age, and much of the so-called Calciferous sand-
.. -. rock and Graywacke of the section, represented as resting on the 1
_ turned edges of the “ Argillite,” are portions of the same series to which
Sei. the “Argillite” belongs. Near the Hudson River a profound fault

ae

¢

2 - 1%n a review of Maclure’s memoir by C. S. Rafinesque it is suggested by him that ‘‘ We must espe- —
~ eially collect and describe all the organic remains of our soil, if we ever want to speculate with the
_ + smallest degree of probability on the formation, respective age, and history |of our strata.” (Obser-
___- vations on the geology of the United States of America, by William Maclure ; a Hotes. Am. :
: Monthly Magazine, vol. 3, 1818, pp. 41-44.) > -
Tae 2 An Index to the Geology of the Northern States, with a transverse section from Catskill Mountain ;
tothe Atlantic. Leicester, 1818. ‘
~ $Katon, Amos. An Index to the Geology of the Northern States, 2d ed., 1820, pp. 154-212.
4Eaton, Amos. <A geological and agricultural survey of Rensselaer County, New York, with ageo-
-Jogical profile from Onondaga to Massachusetts, p. 15, plate. Albany, 1822. Memoirs of the board of _
_ agriculture of the State of New York, 1823, vol. 2, p. 9. ca
‘ 6A geological and agricultural survey of the district ene the Erie Canal, 1824, pp. 30, 66-58 gees
_ plate. oe he

~

-

erm oe nee eee Eo
oa ve ~ ‘ ~~ 4 i ws,
GRANULAR quartz. REReN Se EN

ae ee ¢ sat Prarisvaial erat has forced the Lower Cambrian over and
i the. ‘Silurian (Ordovician) rocks. The misunderstanding of the
u ae relations of these rocks and a dependence upon their lithological
Rear ars led Prof. Eaton into an error that has come down to the

a.

resent day in memoirs relating to the “‘ Taconic System.”

Prof, Eaton reviewed his work from time to time until 1532, when his
il scheme of classification appeared. It is reprinted in the following
abu lation, with the equivalents of his formations as known in the no-

1 nelature of to-day.!

Eaton’s Nomenclature (1832). 1891.
nreorees LiMeroek fools sore oe cde sss. sae Upper Helderberg.
3. ; bregditerous limorock ~.. 62. - 5. see sed.e---. ve-«| Niagara.

2. Millstone grit and rubble Oneida, Clinton, Medina,
1. Second Graywacke slate. Second Graywacke - Utica, Hudson.

Metalliferous limerock.......--...... ee Trenton.
3 MMPOILUrONs SANATOCK 6 5. 1.66 e ewe ecwensecsee cee, Calciferous.
CE NPINGOR, oo. cave ode ns sean aecetsecssue Trenton, Chazy.
{ Lower and Middle Cambrian and Silu-
-Millstone gritand gray rubbl« ? First Gray- J 7
Ct Graywacke slate..........-.. wacke. i Whidaon.
, Roof slate ( Considerable Hudson, but includes a
i Arsen W doke slate > .....02. cceees seeee ee. great mass of Lower Cambrian in
Clay slate | Rensselaer County, N. Y.
. Trenton-Chazy limestone, Calciferous.
3. Granular limerock ....~.-.++-++--+--+-+0+---+- Cambrian limestone.
I ODN. ss. bce whianeducewasdastecc cee Lewer Cambrian.»
1. Granite, Mica slate, Hornblende and Talcose rock | Algonkian, pre-Cambrian, and Ar-

chean.

3 The stratigraphic position of the “ GranularQuartz” (2 of the Primitive)
is correctly represented, and it is now known to contain Olenellus sp.?
Alarge portion of the strata referred to the “ Argillite” (1,of the Tran-
8 spp is. also known to carry Olenellus asaphoides and to belong to the
Lower Cambrian terrane. In the text the “ Graywacke slate” (2, of the
; rransition) is described as resting unconformably upon the upturned
€ Esees of the ‘“‘ Argillite” (1), and it is so represented in the section, Thi
S essentially the same as the section of 1820 and as in the more detailed
Se ection of 1824.

- Rev. Chester Dewey studied the geology of the vicinity of Williams-
town, Massachusetts, and in 1819? published a short sketchof the
D mineralogy and geology of this region. He followed this in 1820 by a
ge seologic section from the Taconie range in Williamstown to the city of

ke

Dit eatczioni Text-book for aiding the study of North American Geology; being a systematic arrange-
‘ment of facts collected by the author and his pupils under the patronage of the Hon. Stephen Van
: as selaer. Second edition, 5 plates. Albany, 1832.

Sketch ofthe Mineralogy and Geology of the vicinity of Williams’ College, Williamstown, Massa-
tte, (With a map.) Am, Jour. Sci., vol. 1, 1819, pp. 337-346.

tion to the mica slates of the Archean are shown, and in a general. way y

tion argillite. In 1824? he described the formation more in detail. -Q .

distribution of the Granular Quartz and its relation to the subjacent 5

_ marble to be the equivalent of the (Trenton) limestone series of the New

sandstone at the base of the same series (the Potsdam sandstone).4 In

> 2A sketch of the geology and mineralogy of the western part of Massachusetts, and a small part of

of New York. Am. Phil. Soc. Proc., vol. 2, 1841, pp. 3, 4 On the physica) structure of the fee

_ generally, Trans. Am. Assoc. Geol, Nat., 1842, p. 482,

“F*
mS) . ~ ” y .
are € et Yi a lg ay: a7, \

oe ere eae, ‘CAMBRIAN. Ree Wp ss ae

Troy, on s the Budacu. In this octane. the relations of the quartz font ma -
the Lower Cambrian slate is described. This is referred to the Transi-

the map accompanying this paper the distribution of the various rock
masses is more accurately given than in any maps published prior to 4
those of Prof. James D. Dana, when studying the strata referred to the
Taconic system. It exhibits an acquaintance with the surface distribu- ;
tion of the rock masses and aclear comprehension of the classification 7
and correlation of rocks on the principle of lithologic characters. The-

primitive rocks, or the mica slate of the map, is particularly well work
out. . gy
Dr. E. Emmons, a pupil of Prof. Katon, adopted the order of succes- 4
sion of the strata as proposed by Eaton, and separated the “ Granular |
Quartz” (2), “Granular Limerock” (3), and “ Argillite” (1) to form a
distinct series of rocks between the “Granite” (1) and the * Gray-
wacke” (2) of the Transition. To this series of rocks he gave the name |
‘“‘ Taconic,” as Nos. 3 and 1 are largely developed in the Taconic range of y
mountains. His central idea was that the rocks were-non- fossiliferous
and beneath the zone of animal life, and were separated by their miner-
alogical characters from the subjacent and superjacent rocks.2 =
In accordance with the belief that the ‘Granular Quartz” belonged
to a system of rocks which were beneath the zone of animal life, re
Emmons considered it the oldest of the sedimentary rocks, and fé
beneath the Potsdam sandstone surrounding the Adirondack mo =
tains. He thus differentiated the Potsdam sandstone and the “Granu-
lar Quartz” as two distinct formations. The work of Messrs. Dewey
sate Emmons added little to the knowledge of the true position of the
“Granular Quartz” in the geologic series, as they did Qh discover
fossils in it or the associated formations. ae)
Prof. H. D. Rogers, in summing up the results of his stale of the
marbles and sandstones of the western portion of Berkshire Count = .
Massachusetts, states that he considered the Berkshire limestone and

York section ; and that the semi-vitrified quartz was equivalent to the

the same year, 1841, a discussion of these formations was publishéd in,
= as

1 Geological section from Taconick range, in Williamstown, to the city of Troy, on the Hudson. A m.
Jour. Sci., vol. 2, 1820, pp. 246-248.

the adjoining States. Am. Jour. Sci., vol. 8, 1824, pp. 1-60.
3Geology of New York, Part 2, comprising the survey of the second goers aries distric ct,
1842, pages 135-164.
4 Some observations on the geological structure of Berkshire, Massachusstts, and neighbecing part

lachian Chain, as exemplifying the laws which have regulated the elevation of great mountain chains

Bees Se - GRANULAR QUARTZ, event it toe 95 - a

4 aon Ree ae <j ry

r of Massachusetts,? ; in which the quartzite is described with ne
In the table on page 303, the “Granular Quartz” is a

we base of the Paleozoic, or Sadimentary Series, that is, at “a

he New York section, modified by metamorphic agency and the in-
trusi on of Plutonic rocks. This correlates the ** Granular Quartz” with
Potsdam sandstone. The * Granular Quartz” and the Potsdam
dstone were referred to the Primal series by Prof. H. D. Rogers?
2 with all the quartzites that were found at the supposed base ot

y ley. ‘This reference to the Primal series is more fully described in
the » final report of the Geological Survey of Pennsylvania.

As Prof. Ebenezer Emmons described the “ Granular Quartz” with con- re
sid lerable detail as the basal member of his Taconicsystem.® Inthere- |
tS s of 1844 and 1847 its occurrence in western Massachusetts and west-
Vermont i is noticed, and it is stated that in all probability itoccurs ‘,
ar north as the Canadian border. Its extension into Vermont had es
n previously noted by Messrs. Eaton and Dewey, and we find in the
a i annual report of the Vermont survey the statement by Prof.C.B.
Adams that a quartz rock constitutes the western base of the Green ae
u ntains from the north partof Addison County to Massachusetts ;
it is further said’ that the quartz rock accompanies the Stockbridge
estone, disappearing with it in the north part of Addison County,
‘that near Lake Dunmore a bowldeér was found in the vicinity of the
rtzite beds containing two remarkable species of Polyparia(?). Two
s later, i in speaking of an excursion into Bennington County Prof. Bs.
ams says that the Quartz rock may equal the Potsdam sandstone, ba

nere has evidently been too great a disturbance in this region to —
‘ rit of certain conclusions.'
eA full description of this formation, is presented under the heading of

oe | the geology of Massachusets, vol. 2, 1841, pp. 560-593.

Mather, William. Natural History ‘of New York. Pt.1, Geology of New York; geology of the
(southeastern) district. Albany, 1843, p. 438. :
On 2 A merican Geology and present condition of geological research in the United States. Am.

Jour Sci vol. 47, 1844, pp. 151-154.

*The geology of Pennsylvania. Philadelphia, 1858, vol. 2, p. 751.

BO! logy of New York, pt. 2, comprising the survey of the second geological (northern) district.
p. 135-164, The Taconic System; based on observations in New York, Massachusetts, Vermont,
ode - Island, pp. i-vii, 67,6 plates, Albany, 1844. Agriculture of New York, vol. 1, pp. 45-112,
1, map. Albany (1846), 1847. American Geology, containing a full statement of the principles
cience, with full illustrations of the characteristic American fossils. 8vo. Albany, 1850, vol.

i ‘Annual Report on the Geology of Vermont. Burlington, 1845, p. 57.

D petal Report on the Geology of the State of Vermont. Burlington, 1847, p 13.

A

“by Prof. C. H. Hitchcock. 1 ‘Detailed Absotidtots are given ~ its chased

Se
ae
‘ we -.,

~~

es yee es
fe & te A ‘, ¥ is

~

be

4%
é
/

Aas
a cat ae
we

eons

4 ‘ £
a

Tah
See

n'y

S% }
y ;
ws

fi ah 9
" ¥ A

®

ponte We

in the valley between Bristol and Starksboro can not be distinguished —
are mentioned as occurring in it; they are: A species of Lingula, a mol-_

_crinoidal columns, the Scolithus linearis (Hall), afew fucvids, and some —
-indeterminable forms which are evidently organic.? The exact seologs

“ Red Sandrock” and “ Georgia Slates” of Vermont. In 1861 the three

_

_ © Final Report on the Geology and Mineralogy of the State of New Hampshire, with contributions *
towards the improvement of agriculture and metallurgy. Concord, 1844, p. 161. a

acter as foundin Vermont, where it is said to have a thickness of at leas 7
1,000 feet.2. On this same page we read that “ much of the quartz rock —

from members of the red sandrock series.” Several species of fossils —

lusk, resembling the Modiolopsis, a straight chambered shell (?), a few —

ical horizon of the quartz rock is not determined. mR
At this point the review of the literature referring to the “ Granula 3
Quartz” will be postponed until it is taken up in connection with the ~

formations were practically united in one geologic terrane by the dis- |
coveries of Messrs. Billings and Barrande and the correlations of the
Geological Survey of Vermont. A review of the references made to
the Red Sandrock and the Georgia Slates will next be given, and 4
then the three formations will be considered together as they are de-
scribed in New York and Vermont. q

When describing the formation terminating the Champlain group of
the New York section Dr. 1. Emmons correlated the brown or red-
brown sandstone of Vermont, on the eastern border of Lake Cham |
plain, as found at Addison, Charlotte, Burlington, and Colchester, with
the gray sandstones that terminate the Lorraine shales of Jefferson /
County, New York.* He thus assigned the “Red Sandrock” of the
future to the summit of the Lower Silurian. ;

In presenting the results of his study of a section crossing Vermont
from the Green Mountains to Lake Champlain, Prof. C. T. Jackson®—
mentions the occurrence at Burlington Falls of a red sandstone con-
Sueerine numerous beds of buff-colored and blue compact limestone des- j

q
‘4
:

RED SANDROQCK.

titute of fossils. He referred it to the Potsdam sandstone of Dr. Em-
mons. ‘ At Willard’s quarry the red sandstone rock alternates with a
bright red slate, covered with ripple marks made by the waters, from
which the sediment was originally deposited.” He further states that
a mile from Burlington, on the Winooski River, large beds of sets be
blue and excellent white limestone are found. 4

Prof. C. B. Adams describes in the first report of the Geological

'Hypozoic and Paleozoic rocks. Report on the Geology of Vermont, descriptive, theoretical, econom-

ie eal, and scenographical, vol. 1, 1861, pp. 342-357. bh

2 Op. cit., p. 355. ; oh a
> Op. cit., p. 356. 4
4Geology of New York, pt. 2,comprising the’ survey of the second geological (northern) district.
- 1842, pp. 123, 124.

.

-

& tare = Pere, ad “/ ~ a” ae
\ " > i Cane .
Pad, Ya Mis a a ee . ty —_

sy aa ao? RED SANDROCK,. 97
ey em .

r : Vermont the occurrence of roofing slates in southern Ver-
wh ich he refers to the Taconic slate of Dr. Emmons, without a
ete to assign them to a geologic horizon.

e following year a section is given of Snake Mountain by Prof.
is? in which the Red sandrock is shown resting conformably upon
tu ison River shale. In 1847 he referred to his studies of the Red
sk’? and noticed the discovery of tragments of trilobites which
ames Hall identified as Conocephalus.* He next: assigned his
ndrock to the Upper Silurian, correlating it with the Medina
one. Dr. E. Emmons criticised this view of Adams, and stated
e was in error. He regarded the formation as of Calciferous or of

sd am age as proved by the fossils, stating that the rocks rest on the
conic slate.® Prof. Adams reasserted his view in 1848,’ stating that no

i

rn

a

eS ee ey ae

ur ntain section showed that it contained Utica “asia Hudson River
_ Later, Dr. Zadock Thompson adopted the view that the Red
dre rock was in its natural position on the summit of Snake Mountain.®
: that the Red sandrock series was the equivalent or the Me-
f the New York section was sustained by Prof. W. B. Rogers?
é Medina or Clinton age of the “ Red sandrock” was supported
Brel gical Survey of Vermont."
ae Billings, on learning of the discovery of fossils in the “ Red
idrock” near Swanton, Vermont, by Dr. G. M. Hall and Rev. J. D.
visited the locality and found a small Theca and a Conocepha-
‘pon this paleontological evidence he referred the strata to about
horizon of the Potsdam sandstone, to which position it has since
| assigned by most authors who have had occasion to mention it.”
ings also corrected the statement of Prof. Hall, that the trilo-
mt Ad the Georgia slate were from the Hudson terrane, and referred
n to o the Primordial or Lower Potsdam. This transferred the Geor-
ries and the associated “ Red sandrock ” to the Cambrian.”
he 5 tind far referred only to the ‘‘ Red sandrock,” as it was men-
ed more definitely, and assigned to a geological position prior to
! aceous and arenaceous shales and slates that overlie it. As
ed sandrock” and these shales or slates will be spoken of together

rst Annual Report on the Geology of Vermont. Burlington, 1845, p. 35.

cond Annual Report on the Geology of the State of Vermont. Burlington, 1846, p. 163.

rd Annual Report on the Geology of the State of Vermont. Burlington, 1847, pp. 13-15.

ne ay certain fossils in the Red sandrock of Highgate. Third Annual Report on the Geology of

f Vermont. Burlington, 1847, p. 31.

ic System. Am. Jour. Agric. and Sci., vol. 6,1847, p. 260.

: conic System.) Am. Jour. Agric. and Sci., vol. 6, 1847, p. 260.

Taconic Rocks. Am. Jour. Sci., 2d ser., vol. 5, 1848, pp. 108-110.

‘of Vermont. Nat. Hist. of Vermont, Burlington, 1853, Appendix, p. 45.

Pies geological structure of western Vermont.) Report on the Geology of Vermont, vol.
6, 327.

C.H. Report on the geology of Vermont. Notes on the sections, vol. 2, 1861, p. 650.

6 of the red sandstone formation of Vermont. Aim. Jour. Sci., 2d ser., vol. 32, 1861, p. 232.

. J. Hall’s claim to priority in the determination of the age of the red sandrock series of

Am. Jour. Sci., 2d ser., vol, 33, 1862, pp. 370-376.

Sul. Sy

‘ wits
aks he BE a ey cee 3 ab sia fob “e ¢ 2 f=
.o = =

pie S . oN Be Oe “ THE ex. oie Baeza ss i we ,

4. Sok ine ry tae Aa

‘; “the latter as mentioned by various authors. ee | Re

GEORGIA SLATES. we nor

The first notice we find of the slates and shales now referred to t
Georgia terrane of Vermont is by Prof. Amos Haton, in 1818.

_ argillaceous and siliceous slates and, in isolated masses, a gray wai :
slate (Nos. 9 and 10 of his figured section) are shown to the east and wes :
of the Hudson River, the slates on the east alone belonging to the Cam
brian.! These siates were referred to the transition class.2 In the ne
edition of his index® these beds are referred to the Argillite (7) and th iT
Gray wacke (9), these terms being then applied to them as seen in Rex
selaer County, New York, and in all of Haton’s subsequent publiention |
It is the Argillite (1) and the First Graywacke or the Graywacke | slat
of the First Graywacke of the nomenclature of 1832‘ and his paper 0 0
1839.5 On Rev. Chester Dewey’s Geological Map of 1824° the sam
area in Rensselaer County is included under the term ee Wacke
and in part * Transition Argillite.” :
In defining the limits of the Taconic Syatem in 1844,’ the northward
extension of Prof. Eaton’s Argillite and Graywacke of Renssela
County into Washington County was called the Taconic slates, and i
was in this series, a mile north of Bald Mountain, that the first fossil il
of the Olenellus or Lower Cambrian zone were found by Dr. Asa Fit eh
These slates, with their interbedded arenaceous layers, formed the Vem
Taconic of Emmons, which he stated could be traced northward. to t
Canadian border. In the map accompanying Dr. Emmons’s memoi OF
the Taconic System, published in 1844, all of the strata east of t th
Hudson are colored Taconic slates, or included in the Taconic system
The same strata in the map of 1842, published by the Geological Sur
vey of New York, are included viniter the Hudson River group. 4 q
Dr. Asa Fitch, a practicing physician in Washington County, Net
York, studied the local geology, and, under the headings of * Taconi

1The Greywacke or Grit area of the eastern part of Dawieate County is now known to be. ab OV

the metalliferous limestone of Eaton or the Trenton limestone series of the New York State Surve}

The recent work of Mr. T. Nelson Dale, of the U. S. Geological Survey, establishes this and prove

that I was incorrect in referring this area to the Cambrian on the map accompanying the paper 0

the Taconic System of Emmons and the use of the name Taconic in geologic nomenclature. (Am

~ Jour. Sci., 3d ser., vol. 35, 1888, pl. 3.) It-is probable that the eastern portion of the Cambrian

as there mapped, to the north of the Berlin Grit area, in western Bennington and Rutland coun Hie

~ Vermont, may also prove to be of Lower Silurian (Ordovician) age. (C. D. W., June, 1891.) a

2 An index to the geology of the Northern States, with a transverse section from Atetsics ;. Mog

‘ tain to the Atlantic. Leicester, 1818, pp. 27-30. A
3An index to the geology of the Northern States. 2d ed., 12mo, Troy, N. Y., 1820, p. 163. i>) ae

4 Geological Text Book, 2d ed., 1832. ; i. ce

5 Cherty lime-rock or Corniferous lime-rock proposed as the line ot reference for State geologi sts

New York and Pennsylvania. Am. Jour. Sci., vol. 36, 1839, pp. 69, 70. ies

6A sketch of the geology and mineralogy of the western part of -ganisn.y nds: and asmall part

the adjoining States. Am. Jour. Sci., vol. 8, 1824, pp. 1-60.

7Emwmons, E. The Taconic System; based on observations in New York, Massachusetts, Ven mon

and Rhode Island. Albany, 1844, pp. i-vii, 67, 6 plates, . , ‘5

4 <

Fah |
eh daa, ‘ . = : ~ =

a soe “GEORGIA SLATES. cr a ie. oe
oie Fes Fe eA ¢

»*

rbedded Daeg with éensiderable detail. He thinks that they
y be ong to an older system than the New York rocks, but no evi-
2e i is s given to support this view. On page 865, Dr. Fitch states that
the s summer of 1844 he found at Reynold’s Inn the first fossils known
m the ne 2 Taconic slate, and sent them to Dr. Emmons, who named and
aed illustrations of two species. Dr. Fitch also describes an
id trail, Helminthoidichnites tenuis, from the “ Taconic slate” of
a rille.? \-
- C. B. Adams, of the Geological Survey of Vermont, called the
rthward extension of the Upper Taconic slate (of Emmons) of Wash-
to jand Rensselaer Counties, the roofing slates of the Taconic system,
cluded them in his Hudson River group.

v ith those of the Hudson River oink and were deniaboned to be
that age. This same view was taken by him of the northward ex-
01 sn 1 of this series in Vermont, when he described the trilobites from
s of Georgia in 1859. At the close of this article he says:°

d | % to the evidence heretofore possessed regarding the position of the shales
in ng the trilobites, I have the testimony of Sir W. E. Logan that the shales
bis ‘is locality are in the upper part of the Hudson River group, or forming a part
fe series of strata which he is inclined to rank as a distinct group above the Hud-

Ste It would be quite superfluous for me to add one word in support
nion of the most able stratigraphical geologist of the American continent.

r bs H. Hitecheock,® in speaking of the trilobite rock of Vermont,
mv Syhich Prof. Hall’s specimens were obtained, stated that he con-
od them as overlying the equivalent of the Oneida, which was
cent to the Hudson River Rocks.

@ attention of M. Joachim Barrande having been called to the
found i in the Georgia slate, he studied them with great care, and
lishe ad. an extended review of the literature referring to them, and
ed the paleontologic proof of the age of the rocks.7?. He decided
‘the e fauna was equivalent to his Primordial fauna of central Bo-
a. ina that it could not be referred to the Second fauna, as had been
ine American prmervers. Under the impression that Dr. Em-

: | Topographical, and Agricultural Survey of the County of Washington. Trans, N.Y.
fees. for 1849, 1850, pp. 830-857.
DU Report on the Geology of the State of Vermont, Burlington, 1845, p.61. On the
s, Am. Jour. Sci., 2d series, vol. 5, 1848, pp. 108-110.
fology of New York, vol. 1, containing descriptions of the organic remains of the lower di-
» New York system, 1847, pp. 252, 256,257.
upon the trilobites of the shales of the Hudson River group. Paleontology of New
applement to vol. 1, 1859, p. 529.
ology of Vermont, chiefly in connection with the Taconic System. Boston Soe. Nat. Hist.
L7, 1861, pp. 426, 427.
eas et nouveaux sur la faune primordiale et le systéme taconique en Amérique,
2, Bull, 2e sr., vol. 18, 1861, pp. 203-321.

fe

* a : < a] in
a" 5 ; can roe — ‘ F ; A .

t erat SPR vy od sige Aste ‘ matte oS fr ae ears “yes, ee NS 5 P.
= a! > ’ ‘ , ’ Be

‘
‘ rug

changed his views in relation to the age of the rocks containing Ole

My

‘i

+ gh ise Sin Hee “me ‘CAMBRIAN. = ae eas 24

other places; that at no point where the Potsdam sandstone is seen i

schistose rocks; that he has always referred it without hesitation to tl th

the Potsdam sandstone seems to be that of an upper formation. — ti

the supposition that the sandstone is the upper rock. He then quot te

? : = oe
any FF (3 sto. Ss

~ Tintd - y ~
3 . ae

‘mons’s Media rants work was correct, M. Bantants credited him wv ‘itl
having correctly located the Primordial fauna in America, Se

In 1861 Prof. Hall changed the reference of the Georgia trilobite
- from the Hudson River group to the Quebec group. Ina letter writ
ten to M. J. Barrande, dated April, 1862, the explanation of this is given.
He states that his own conviction was that the Red sandrock an¢
the Granular Quartz of Vermout were of the age of the Potsdam sand-
_ stone and that the schists and shales which held the trilobites belong
eatwooh the Potsdam sandstone and the Trenton limestone. He the

nellus and other trilobites, and referred them to the lower portion ¢ 7
what is now designated as the Silurian (Ordovician). He says: g

You will understand, then, that if my views touching the relations of these ro ck
are exact the valley of the Hudson River from the high lands on the south of Lak é
Champlain, save a small uumber of inconsiderable exceptions, is occupied by rocks
of the Primordial zone, that is, by rocks placed between the Potsdam sanidatone sa T
the Trenton group. Thus the Hudson River group in its typical localities belongs t
the Primordial period.? apa a2)

In explaining how he came to adopt the view that the trilobies Tron
the Georgia slates of Vermont and those described by Dr. Emme ns
trom the black slates of Washington County belonged to the Haam Or
River group, together with cut strata in wruok they were contained, }
Says: on 4

I wish to claim nothing for myself or for my former views, for we owe s the 1 a
solution of this question to the Canadian survey. Yet there remain some diverge m1
_vViews in regard to the relation between the shales and the Potsdam sandstone.

He further states that this arose from his seeing the Potsdam sa:

stone run beneath the slate at Whitehall, New York, and a ee D

there any shale or other formation beneath it, excepting the crystallin
rocks of the Adirondacks. Speaking of the “Granular Quartz,” he say
that it presents the same relation as the Potsdam sandstone to thi

Potsdam Sanaaroaks He held the view that the schistose rocks, wi
their impure sandstones, brecciated limestones, and calciferous sané
rock, are to be placed between the Potsdam sandstone and the Trent 1
limestone group; that the relation of this group of sehists or slates t

none of the outcrops that he saw in the disturbed region east of: h
Hudson was there one that could explain the phenomena presented, 0

the nomenclature of Eaton to show that it was almost the same as | tha
finally adopted by the Geological Survey of New York, that is, the ord
of superposition of the formations, the ‘*Granular Quntis? being place
at the base. It is also stated that the graptolites found i in the bee

iGosrnetion for the thirteenth annual report. 14th Ann. Rep., State Cab. Nat: :Hist., 1861, p p.1
* Letter on the Sangre of America. Soe. 60. France, Bally 2e pines vol. 19, =e P. 732,

sm ENeiated ‘slates and arenaceous eds under the title of
. In proposing the name Georgia group to designate
Prof C. H. Hitchcock said :?

im ze

oe County, where it is developed in its full proportions and where the most
x fossils have been found. It is a name also which does not involve any
and dmay be used by both parties in the controversy respecting itsage. * * *
gia e slate includes. what Prof. Emmons has ranked as the black slate, Ta-
€ and roofing slate; and yet not altogether, for we have regarded all the
beneath the red dataset as belonging to the Hudson River group. The
is tic trilobites of the Georgia slate are represented by Emmons in his Ta-
te om, 1844, as found in the black slate.

ollowing fossils are cited as characterizing the Georgia slate in
no it: Barrandia thompsoni Hall, B. vermontana Hall, Bathynotus

n species of fucoides.°
atigraphic position of the Georgia series was considered to be
ae Sandstone which represented the Oneida conglomerate, and

1 of the stratigraphic position of the faunas found in the
| slates by Prof. James Hall, Sir William Ei. Logan, and M. J.
" accompanies the chapter. <A fair presentation of the argu-
‘and against the Silurian age of the terrane is given. Ina
pee trilobites of the shales of the Hudson River group, in

Vit Sisk bait of the iotliers AeA of the State.
bing the rocks of Waterville, Maine, Prof. C. H. Hitchcock®
the slates are similar in mineralogical structure to the

Bement rocks. Report ov the geology of Vermont, vol. 1, 1861, p. 358.
ee _ 4Op. cit., p. 366.
tou the geology of Maine. Preliminary Rep. on the Nat. Hist. and Geology of Maine.

>. 233

ant eo - ononata ‘TBRRANE. Mee a ee SOR

term Georgia group to designate this terrain, from the town of Gouigis :

Hall, Graptolithus molest Hall, the trail of an anette: and

ess of the slate was thought to be at least 3,000 feet. A.

Wet Ae cap Meee LS “THE CAMBRIAN. ARTS foun a,

oe Vermont, Mr. E. Billings states that Mons, Barrande first determined ©
their age.’ He further says: i ha

_ the Scolithus is identical with that which occurs in these two States, and some por-_

_ group.2 In speaking of the élaim of Mr. Billings, that he had identi- F
-. fied the Primordial fauna in the Red sandrock and determined its geo-
logical age, Prof. James Hall‘ states that he had published sections and.

considered them to be of the age of the Potsdam sandstone of the New

- glates, where they are recognized by Prof. Hall as belonging to the
Potsdam. On the contrary, they are marked on the section as belong re
‘ing to the Trenton-Hudson series. :

- 421-122.) .

Bt tat No eS ee a :

ine: ret" be, PSs ates ys
Chae a5 " Sa Ph tn eT he ne as
5 St - " . . "

cl
Ast (a

: . ” cs °F)
fossils in the Mississippi Valley, was also referred to. the Primordial :
the review of the history of. these three Cambrian. formations as. they
appear in New York and Vermont is carried forward as that of one ter-—

rane. . 4

In speaking of the determination of the age e of the vinta’ in Georgia,

4

At the time I wrote the note on the Highgate trilobites it was not known shail

these slates were conformably interstratified with the Red sandrock. This discove pe

was made afterwards by the Rev. J. B. Perry and Dr. G. M. Hall, of Swanton. _

He also mentions the discovery on the Straits of Belle Isle, by Mr. J. —
Richardson, of the Canadian Geological Survey, of Scolithus linearis,
Paradoxides thompsoni, and P. vermontana, and a number of other spe- :
cies of which a list would be given further on. He adds:

The sandstones and limestones of the north shore of the straits [of Belle Isle] ipo
pear to be of the age of the Potsdam of Pennsylvania and Tennessee. The form of

tions of the rock is a coarse red sandstone, exactly like the specimens sent to. me ¥
about a year ago from Tennessee by Prof. Safford. , _ “=

Mention is made of the discovery by Rey. J. B. Perry and Dr. G. M
Hall of a group of fossils interstratified with the Red sandrock east of
Swanton, Vermont. Of the species found, four occur in the limestone
which overlies the sandstone with Scolithus linearis on the north shore
of the Straits of Belle Isle. _

Taking all these facts together scarcely anything more is necessary to show that.
the Red sandrock of Vermont is of the age assigned to it by me from an examination
of Conocephalites at Highgate in July last. * * * Barrande’s opinion, founded |

altogether upon the aspect of these trilobites is thus completely verified.2 _ 4

At the close of the paper is a list of the fossils found in Vermont ar id
on the Straits of Belle Isle, all of which are referred to the Potsdam

made statements in relation to the age of these rocks to show that he

York section. In reply Mr. Billings® said that the sections ‘piketal
by Prof. Hall do not cross at any point the Red sandrock or Georgia

= or

1 Further observations on the age of the red sandrock formation (Potsdam group) of Canada a nd
Vermont. Am. Jour. Sci., 2d ser., vol. 33, 1862, pp. 100- 105. (See note and corrections, same rol B De

<i

2 Op. cit., p. 102. 3 Op. cit., p. 104. ~
4On the Potsdam sandstone and Hudson River rocks in Vermont. Am. Jour. Sci., 2a ser., vol. 33,
1862, pp. 106-108.
5On Prof. J. Hall’s claim to priority in the determination of the age of the Red ae mee
Vermont. Am. Jour. Sci., 2d s6r., vol. 33, 1862, pp. 370-376. “yy ee aden ie

/

, « , % mS A eet ow ~~ i — r Lali. 4 j oS. sl
if bt vrs +f a) \ t- we oe ba se Z = ‘aa’ Lee ‘ 7
% t < > wit ty ia . +>. 4, : r
A Ge we Bese = ~~ aE ait yt
».» ay - * ’ 4 tw ye ‘
Pre / 4a i wipe Se . ay -
nals x cn ; “ = : .
wal a Bee
rey - >
Rey - GBORGIA TBRRANE. 103
S

Aha Retiasein g the ieniutions that occur north of the Vermont and Can-
la seen to the southward, Sir William B. Logan studied a section
ithe v vicinity of Swanton, Vermont, in which the Georgia slates and the
( allus fauna occur above the Red sandrock.' The latter are red and
white dolomitesin sandy layers. The measurement of this section gave

a th ickness of 710 feet, including 190 feet of shale, carrying the fossils
wi hich ope Billings described. He traced the rocks of the ea yee: sec-

of the hie secehcne. The name Red sandrock is a misnomer, as
2 is in reality comparatively little sand or arenaceous material, other
ec stion.

- Prof . Jules Marcou took a very active interest in the discussion of
he sti tratigraphic position of the fauna found in the slates of Georgia,
nont, and published numerous papers upon the subject from 1860
388. In a paper published in 1861 he records some of his own
rvations, saying that in Vermont the Potsdam sandstone has ex-
etl 7 the same aspect and composition as at Potsdam, in the State of
New York. Near Saxe’s Mills, a mile east of Highgate Springs, it con-
fains two species of Conocephalites, C. adamsi and 0. vulcanus. He
ta S s that the formation is adeese up into narrow bands aisha are

* Below the Potsdam sandstone lie great masses of slate, four or five
and feet thick, which for convenience I should divide into three parts.4

Tt ‘hese are the Lingula flags, Georgia slates, and St. Albans group.

r notably Paradowides (Olenellus) thompsoni, P. vermontana, Peltura
| lop, yga, Obolella cingulata,-ete.

In noting the discovery of fossils in the Winooski marble, at Swanton,
Ter rmont, Mr. E. Billings ® states that fossils were discovered by Mr.
a Allis, of Burlington, Vermont, who sent them to him for ex-

epotey of Canada; report of progress from its commencement to 1863. Montreal, 1863,

oa pp. 145, 140. ca ee Nat., new ser., vol, 6, p. 351, ;

wan
ad ,
P ig s
a or Sie
we Ae ey ee ae he 2 ee

the n arenaceous limestone of a highly dolomitic character, in the entire

e Georgia slates are stated to be characterized by Primordial fos-

a ae

Sakiatioe. He fond a species of ena which he identified

‘Swanton and St. Albans, seems to underlie the Georgia slates, and he
i a . ; . g ;

lates the formations of that State.’ The Potsdam group is made t

Georgia slate, most of the quartz rock, and the Potsdam sandstone of

that the Potsdam sandstone accumulated along the shore, while shal eS
- and limestones were accumulating to a greater thickness in the deeper

age of the rocks of western Vermont he says: ‘ att

: affords no proof of the existence in Vermont of any strata (a small spur of Lauren-

Py ES oye es ne = he meets AY
Pe ~ ape ge a “we eG te oe Ee
“104 nee a at a
eh et = “THE cAMBR AN. ap Sahat en

Salterella pulchella. He observes that the Winooski marble, both ¢ ut

It is gicnerally of a reddish, mottled color, but sometimes gray or greenish. The o
limestone at the Straits of Belle Isle, in which 8. pulchelta i is found, is also red, gray
and greenish; and is, I have no doubt, of the same age. At this latter locality i
overlies a red or brownish sandstone, conformably, which holds Scolithus linearis. ’
consider the Belle Isle sandstone to be the “ Quartz rock” of the Green Mountains of
Vermont. In that case, the limestone at Belle Isle occupies, stratigraphically, the
position of the Stockbridge limestone as represented by Dr. Emmons in his American
Geology, part 2, p.19.! a” 4

Under the title “Geology of Vermont,” Prof. ©. H. Hitchcock tabu-
include the Red Sandrock, part of the Hudson River slate, part of | the

West Haven. -Speaking of the latter be says, the Potsdam rocks flanl i
the gneiss upon the west side as far north as Middlebury. He further
observes that the quartz rock is probably the same as the red sandstone ;
that both are overlain by the Levis? limestone, and resemble each othe :
very much near their supposed union. “TI find this view of the identity:
of those two formations confirmed by the late map of the Canadian s Ir
vey, published in 1866.” aE

In an article on some points in the Goitine of Vermont, ‘Dr. ca
Hunt states+ A

It happens, then, from the facts already set forth, that the Potsdam formation,
which at its outerop at the foot of the Adirondacks and Laurentides includes o} y
from 300 to 700 feet of sandstone, is represented a few miles to the eastward by nol
less than 2,000 feet of dolomites, sandstones, and slates, and moreover that ocenpy- -
ing a position between the calciferous and chazy formations, which are contiguot us
at their eastern outcrop, there becomes intercalated within this short distance a fe s
siliferous group, several thousand feet in thickness. a

‘The explanation of this is quoted from Logan’s opinion, to the off

water of the adjacent ocean. In summing up the evidence as to the
. ..
ee.

All the evidence, paleontological and stratigraphical, as yet engin forws rd

tian excepted) lower than the Potsdam formation, which the present advocates of 3
the Taconic system regard as forming its summit. * * * That strata still older

than the Potsdam of New York and Vermont were deposited in some portions of th he
oceanic area is apparent from the existence in New Brunswick of the St. John’
slates holding a Primordial fauna older than the pee and it is not impossible e

10p. cit., p. 351. 2 Am. Assoc. Proc., vol. 16, 1867, p. 120.

’Levis group, including the ‘‘ Kolian limestones,” ‘‘ Hudson River Hmgstaaies; ” and the greater po
tion of the Georgia slate. (Op. cit., p. 120.)

4On some points in the geology of Vermont. Am. Jour. Sci., 2a ser., 46, 1868, Bs 225,

* se ee > .
a Xs 2 eA n wet ay | —
: ie elt Sp Y : ~~

ven nts may underlie the Potsdam formation of Vermont. No such
b Mov jowever, as yet been detected in either Vermont or Canada. !

Hunt ‘also confounded the typical Potsdam sandstone of
Adin pidaicks; the quartzite of the western base of the Green Moun-
and e Primordial series described by Murray in Newfoundland

oat his statement that a few hundred feet of typical Potsdam
2 in New York are represented in Vermont, Quebec, and New-
1 by tl thousands of feet of strata lithologically very unlike the

: Fi ‘ 33 wre.”
1867 Prof. Cc. i. Hitchcock identified the Winooski marble of
9 os t as the Red Sandrock, and stated that Olenellus thompsoni and
a

ontana occurred in the superjacent slaty layers. In the same
_ he presents a table of the strata from the Silurian to the De-
1, inclusive, as found in Vermont, and in this connection he says
; ae the Taconic to be of Lower Snes age. This included,

uivalent to the Potsdam, and that the sedimentary beds below

of Barrande. The Potsdam is considered to be the top of the
dial, not the base of the Silurian. In the table of formations
| sandrock or Potsdam is placed at the top of the Taconic sys-
n, and the Taconic slate with the quartzite limestone or conglomer-
at the base. The following year the same author® again stated
he 2 Red sandrock was of Potsdam age and not Medina, and he
ded the slates below into the Swanton and Georgia series, as
thi an uP eae. slate, referring them to the Primordial of Bar-

U mmary of the Geology of Vermont, by Prof. C. H. Hitchcock,?
d in connection with the Geology of Northern New England,
d, under the head of “Potsdam Group,” that it includes (1)
: ate, or part of the “‘ Hudson River slate” of the former report
Vermont. Survey. (2) Georgia slate. (3) Red Sandrock and
rock at. the base of the Green Mountains. (4) Potsdam sand-
pe sine. as the original beds in New York.

s a
Ae

ole ogy of eastern New England. Am. Jour. Sci., 2d ser., vol. 50, 1870, p. 85.

oski marble of Colchester, Vermont. Am. Assoc. Proc., vol. 16, 1867, p. 119.

ay of Vermont. Am, Assoc. Proc., vol. 16, 1867, p. 122.

s0¢. Proc., vol. 16, 1867, pp. 128-134.

on the red sandstone of Vermont and its relations. Boston Soc. Nat. Hist., Proc., vol.

. ih

DR pee eee PEA yt erg ee

: Satis eOROTA TERRANR. ee . 4 : 104 :

} ad: on Mr. ApS Perry. He concluded that the Red sandrock

sdam were not Utica or Lorraine, but belong to the Primordial — |

PSE NS Be a OTR AE a eet aa Ne SPER a gg
D rah b. 1 MN. Seg 2 SD ESCs ee ee ee Oo it, nee
i pay 2) eee egy Sigg ae eas act
‘ es AK ak x a5. » Sand Cine pened Se ae ee nary AY au & ?
” . “ot ? * - ae on At
1Geg hs THE CAMBRIAN. ee...

‘The Red sandroaks 1S Sikaunttid as extending froin St. Armand, prov-
Sy ince of Quebec, to Bridport, Vermont. AD ‘ ‘a
ey - ‘The brightest red rocks are found along the western border; so that wee the allix te,
~. ance of the red rock of Burlington and the quartzite of Bennington seems incongru--

ous, it is otherwise with the reddish rocks-of Monkton and the brown quartz of
_ Starksboro’ and Bristol. 3

E>
~

| It is stated that the name. Georgia was applied to the group of slate
- _ earrying Olenellus. It was then supposed that the slates were entirely
-- distinct from the sandstones, but further investigation has shown an
ah -interstratification, with the presence of the characteristic trilobites q
throughout the beds. > a
ss Of the “ Granular Quartz” on 1 the western slope of the Green M oun
tains he says: 33 ae

Fh No rock can be more distinct from all others than the quartzite froth the State
line north to Starksboro’, consisting chiefly of pure vitreous silica, sometimes hardly.
showing a sedimentary composition. * * * The group makes a mountain range
throughout, some of the peaks exceeding 3,000 feet in height. * * * An abun- 4
dance of Scolithus linearis appears in this formation, and the rock was referred to the
Potsdam in 1841 by H. D. Rogers and W. B. Rogers, in oppositign to E. Emmons, who

subsequently called it ‘“‘ grannlar quartz,” lying at the base of the Taconic system,
_ thousands of feet below the former.! <a 4

‘In 1871 Mr. S. W. Ford? published an account of a section of see at

- Troy, New York, in which he had found the Olenellus fauna. In 1884,
; he added? a description of a section near Schodack Landing, south o1 ry
_ Troy, in Columbia County, New York. By the contained fauna the yh

ee strata were correlated with those described by Sir William Logan, i in
“i aaah Canada, and Newfoundland.
Prof. J. D. Dana,‘ from 1872 to 1877 worked out, with considera

detail, the stratigraphic relations of the “ Granular Quartz,” of Berk-

_ shire Aeunty, Massachusetts, to the subjacent Archean and the super-
ee Silurian limestone, adding many details to the general outlines”
published by Messrs. Eaton, Dewey, and Emmons. In the description
of the quartzite, limestone, and associated rocks of Great Barrington, |
3 Berkshire County, Massachusetts,‘ it is stated that the quartzite of Great 4
_ ~ Barrington alternates with mica schist, and that both of the rocks fot :
¢ the most part overlie the Stockbridge limestone. Of the Green Moun- *
tain quartzite, Prof. Danasays:® “In the first place there are quartzites
of more than one age in New England, west of the Connecticut River.” ‘A

. s a
2a

“ 1Op. cit., p.3. Bs
2Notes on the Primordial rocks in the vicinity of Troy, New York. Am. Jour. Sci., 3d ser., vol 2,
1871, pp. 32-34. Can., Nat., new ser., vol. 6,1872, pp. 209-212. —.. 4
3On the age of the glazed and contorted slaty rocks in the ee of Rohedenk k Landing, Rensselaer
County, New York. Am. Jour. Sci, 3d ser., vol. 28, 1884, pp. 206-208. .
Green Mountain geology. On the quartzite. Am.Jour.Sci., 3d ser., vol. 3, 1872, pp. 179-186, 250.
Ree: 256. An account of the discoveries in Vermont geology of the Rev. Kugadiieis Wing. Am. ioe
_~ Sei., 3d ser., vol. 13, 1877, pp. 332-347, 405-419; vol. 14, pp. 36-37, 1877.
oe 5On the quartz, iikbetans and RARE rocks of the vicinity of Great Birgit, Berkshire
Sy County, Mass. Am. Jour. Sci., 3d ser., vol. 4, 1872, p. 362.
Green Mountain geology. On the quartzite. Am. J our. Sci., 3d ser., vol. 3, 1872. p. 181,

= ) ; "- “ee

a Src fo hie tot i eR A la ae 8 aie EE pee) Ae
* AE) y sf Xe hae 4 4 ‘
Pro Paes hee
hee’ - R
a Se | OronarA TERRANE. 107

’ t

en Paaanbain range, whose relation to the quartzites jntovnedited
i’ fy is unascertained. ‘“‘ We can not assume, therefore, that
lis last is all of one geological age.” After examining the quartzite of
a Connecticut, he was led to the conclusion from the facts observed
2 oe is the inferior rock, and rests unconformably beneath

states that Dr. Emmons believed the rocks were deposited against
estern base of the Green Mountains, in order of, first, the Granu-
uartz, then the Stockbridge limestone, and lastly the various slates

iy

hich were capped by the black slates holding Olenellus, The report
ys s further: :

. Hitchcock suggested as a better theory of structure, that sediments were formed
nporaneously, both upon the Green Mountains and the Adirondack side of the
, thus making the granular quartz on the east side of the valley of the same

th the Potsdam sandstone at Whitehall, N. Y., and elsewhere west of Lake
plain. ‘Next, the Calciferous sandstone, Levis, Chazy. and Trenton limstones,

jacent to both the quartz rock and the typical Potsdam sandstone. Thirdly,
estones are succeeded by pig This theory of original ee differs from

© are, is regarded as Paasagm (or Primordial) in age, because it contains in
s Scolithi (worm-burrows) and Fucoids like those foun in the Potsdam

on the stratigraphical structure of the Cambrian and Cambro-Silurian rocks of western
Boston Soc. Nat. Hist., Proc., vol. 18, 1875, p. 191.

oe of the Cambrian of western Medio Prof, Bap Hiteh- :

j because also it adjoins Calciferous pmneetnae beds at the localities just

Dr. se 2 Hunt, in 1878,! gives an dint @ridal review of ‘the rocks re:
- ferred to the Cambrian Ste." Taconic systems and i in this way speaks ¢ of
the “ Upper Taconic” and refers it to the Cambrian, and the Graniiel 4
~ Jar Quartz” to an Archean system. Again, in 1883, ~84,. ~—86, he went
over the same ground,’ but did not add any original intopaaince Upon 4
i the subject. He adopted the view of Prof. Eaton so well expressed in 4
~~ the section of 1824, and brought down to 1886 the erroneous view of the
SH unconformity Gacwean the Calciferous sandrock and the Argillite. To |
the strata which Dr. Emmons included in the Taconie system, in 1842, —
% he gave the name Taconian, referring them to a pre-Cambrian, Archean, | 4
-_- group of rocks. “4
ao In a paper upon the colonies in the Taconic rocks of the borders of
- Lake Champlain,’ Prof. Jules Marcou gives a résumé of his investiga- —
tions in northern Vermont up to date. In the vertical section accom- —
-_-panying the geological map, the Potsdam sandstone is placed at the —
summit of the upper Taconic series, and then in order below, the Swan- — ‘3
- ton schists, Phillipsburg group, Georgia schists, and the St. Albans
- group. On sections in the text the Potsdam sandstone is represented |
: as unconformably superjacent to the Georgia slates, the Phillipsburg — bi
group, and the Swanton schists, and the St. Albans group. A general —
description is given of the formations as interpreted by Prof. Marcou. — |
As now known the Potsdam sandstone as identified by him, is the Reé iS
_ sandrock of the Vermont geologists, or the arenaceous magnesian lime- :
stone of Logan. Its stratigraphical position is at the base of the series |
_ described, or at the base of the Lower Cambrian as now understood. —
Beha A series of geological sections across Vermont and New Hainpehieas
i _ _ by Prof. C. H. Hitehcock* have the Red Sandrock series marked as-
7 Potsdam and the Georgia slate series as Cambrian. The Granular. a
_ Quartz of the southern portion of Vermont is all marked Potsdam. — De
~~ the text? Prof. Hitchcock says: 2

>

Three bands of sandstone therefore are referred to the Potsdam in the Champlain
: valley: first, the normal gray sedimentary beds at the foot of the Adirondacks, ©
; always known under this name since 1840; second, the quartzite on the flank of the ©
Green Mountains; third, a range of red Saati and dolomite from the Canada 4
line to Bridport, here it is succeeded by outcrops of a material not distinguish-
; _able from the first named band. Partly accompanying the middle band is a series of —
slates and hard sandstones, passing into roofing . slates. called the Georgia group 1 in
the State report, which carries such fossils as Olenellus and Angelina, and is, there-
ere ria thought to be somewhat older than the typical Potsdam sandstone. » am
Bae. In the same publication Prof. R. P. Whitfield® states it to be his

a

ae a ae Special report on the trap dikes and azoic rocks of southern Pennsylvania, 2d Geol. Surv. Pa. jE
1878, p. 253. ’ ag
os 2The Taconic question in geology. Mineral Physiology and Physiography. A second series ¢
in chemical] and geological essays, with a general introduction. 1886, pp. 517-686.
ile 3 Sur les colonies dans les roches taconiques des bords du see Champlain. Soc. géol. France, Bull Sy
tet gme gér, vol. 9, 1880, pp. 18-46. i
he 4 Geological sections across Vermont and New Hampshire. Am. Mus. Nat. Hist., Bull., vol. oP 1
pp. 155-179. - .
“6 Op. cit., p. 160. <a
6 Notice of some new species of Primordial fossils in the culldcitehie of the Museum, and correct ne
of previously described species. Am. Mus. Nat. Hist., Bull., vol. 1, 1884, P. 140. “ | besa Suan Cs
‘ a ee a

~—
~
mp vot
$F es
—

=, : ~

Sa ‘a Se Aa FE ONG AD OSS ee

She ee Pe S SAREE nk Reps eae Pt peeling A RAs
Dea eaten a Se Se A a, * ~~
a | @pORGIA ‘TERRANE. ee 109

owel er prdon of the Wisconsin series; and that the Acadian beds
| pada and Vermont, and perhaps the other Atlantic areas, are not
eciably different in age; but the difference in faune is more the
. upon which life depended than a difference in time.
enefalization of Prof. Whitfield placed the (‘Granular Quart Zz,”

a an Prof, N. H. Winchell! iieelniad the ** Granular Quartz” of
Emr n0ns’s Taconic system with the Potsdam sandstone, and mentions
V estward extension in the Mississippi Valley. In another paper? he

‘ that the eee arr ical relations of tad ty Granular Quartz” and

1 : Potsdam ; that the Red sandrock overlies the Georgia uncon-

ihe Potsdam sandstone to the asap are pe puget as those of a

; oo he inferred from the be ‘cil apueronk conforma-
hat its age was Potsdam or that of the lowest beds of the Lower

estone that ae the limestone conformably, and is an inde-
ot formation and newer than the limestone. In his stratigraphic
lusions at a later date® the Cambrian quartzites are supposed to be

4
IPs

immediately adjacent to the Archean gneiss and equivalent to

stone are supposed to belong to the Hudson period.

paper on “The Taconic System and its position in stratigraphic
e Prof. Jules Marcou® tabulates the strata referred to the Taconic
in eastern North America. In this, the Saratoga limestone,
dik kellocephalus is the summit of the series, above the Red sand-
4 Vermont and the Potsdam sandstone of Keeseville, New York.

stating 1 rocks of Sintiodots: Lspicent caneit of ecohease made in the study of their field
Statement of problems yet to be solved. Geol. and Nat. Hist., Survey of Minn., 17th Ann.

ic ¢ rocks” and stratigraphy, with a geological map of the Taconic region. Am, Jour,
iiecokd ea Ateninraphy; with a geological map of the Taconic regions. Part 2. The

orthern part. Am. Jour. Sci., 3d ser., vol. 33, 1887, pp. 408-409.
b Piss. vol. 20, 1885, p. 224.

nably, and that the stratigraphic relations of the Granular Quartz

nof the region; also, that there is a quartzite west of the border of ©

tsdam sandstone, while those that occurred at a horizon above —

stone) and the base of the Gambrian (the Red sandrock of Vermoul

er a. Tt My. ek = eee ae ae: ) rae ay yy Pie
Diep eer a uke ar eI

10” es eS a THE “CAMBRIAN, a node

het

.3 ae order, below; comes fhe. Swank slates, aad the Phillipsburg!
~ Point Levis group, subjacent to which are the Georgia slates (or Ole-
nellus zone). The Paradoxides zone, the Upper Cambrian or Eophyton
--sandstone of Great Bell Island, Newfoundland, and the Aspidella — a“
Arenicolites slates of St. John’s, Newfoundland, are assembied under r
the name “ St. Albans group.”
In this table, under the upper formations or “ Potsdam grown? there
are brought together the summit of the Cambrian (the Saratoga lime

as well as the Keeseville sandstone, which is the lower portion of the
Upper Cambrian. In the “ Swanton slates ” (Trenton-Hudson terrane)
and in the “ Phillipsburg or Point Levis group,” we have the Calcif-
~ erous-Chazy zone. The Eophyton sandstone placed beneath the Georgia a
slates and the Paradoxides beds is the equivalent of the Saratoga lime-
stone placed at the summit of the series. The Aspidella and Arenicol-
ites slates of St. John, Newfoundland, are of pre-Cambrian age. Thus S
the lower or “St. Albans group” includes pre-Cambrian, Upper Cam-
brian, and Paradoxides zone strata. :

In an article on the Winooski or Wakefield marble of Vermont Prof. ei
G. H. Perkins! described several sections of the strata containing the
quarries worked for marble, one of which has a thickness of 1 410 fee
another 790, and another 710 feet. He found Saltereila ‘ptslohaltins in t the
~ marble bads and considered the series to be of Primordial age. ee

- When describing a section in the Cambrian formation of western
Vermont in the town of Georgia, Franklin County, Mr. C. D. Walcott
stated that the section consisted of a massive belt of limestone 1 ,000
feet in thickness subjacent to a series of argillaceous shales, at the bas 6
of which the Olenellus fauna occurred. He also stated that this sectio n
includes in its vertical range the sections above and below Troy, N. Y.,
- in the Hudson River Valley, and those of Newfoundland and the Straits
of Belle Isle. This was followed in the same year? by a detailed de
scription of the Georgia section, and another section taken near |
Canadian and United States boundary in the township of Highgate a.
_At this latter locality the Red sandrock series has a thickness of 1,170
feet; the Georgia slates a thickness of 1,000 feet. A list of the fossils
praieine in the strata is given in the tabulated section. Followi ng
the nomenclature proposed by Sir William Logan, the Red sandrock
_ series and the Georgia slates are referred to the Middle Cambrian sub D:

jacent to the Potsdam sandstone of the Adirondacks, and above che
Paradoxides slates of New Brunswick.‘ In the same year he det er-
mined by paleontological evidence that the roofing slates of Granville,

1Am. Naturalist, vol. 19, 1885, pp. 128-136. a a
2Classification of the Cambrian System of North America., Am. Jour. Sci., 3d ser., wok 32, 1886, pl
-3Second contribution to the studies of the Cambrian faunas of North America. U.S. Geol. Surv ve 7
Bull. No. 30, 1886, pp. 13-20, ,
4Op. cit., pp. 63, 64.

asese “ GEORGIA TERRANE, 5 hvac iit:

‘ os or,

he same geologic gion as the Georgia slate.!

‘Dutchess County was described by Dr. W. W. Mather? as it

about | Stissing Mountain. He refers,to it as the “Granular
and Potsdam sandstone. Within a few years Prof. John ©.

Raid that no 0 fossils ad: been found in it. In the description of

oo

ri mn ordial rocks of the Per age Valley, by Prof. W. B. Dwight,‘

abate Rby daccett Bad Mr. C. D. Walcott of Middle® Castine

1s i the arenaceous quartzite and limestones on the flanks of the
De It is thus correlated with the Olenellus beds of the Georgia

yf Vermont.

th he Ann Arbor mabe tine of the American Association for the

val ae ement of Science, held in August, 1885, Prof. Dwight® an-

neec | the discovery of fossiliferous Potsdam strate at Poughkeepsie,

Ye Pk... EH 7
pxor be € Says’:

ervescing freely with acids. It is also everywhere more or less arena-

) » sand as they decompose. —
< passes on the « one hand into a smooth fine-grained, ene ee PERE

mn species of fossils are given. This paper was subiaeet more in de-
“a he peenier of the American J ournal of Science for -Febraary,

. ee announced in 1889 the Sass of fossiliferous strata

.D. Cambrian age of the roofing slates of Granville, Washington County, New York.
Proc., vol. 35, 1887, pp. 220, 221. (Advance sheets published 1886.)
ttt of New York. Part 1. Geology of New York; Geology of the first (southeastern)

2

bany, 1843, pp. 418, 423, 436, 437.

York. Thirty-ninth Ann. Rep. State Mus. Nat. Hist., 1886. pp. 166-185.

‘rocks of the Wappinger Valley limestones and associated strata. Vassar Brothers
vol. 4, 1887, pp. 206-214, Discovery of additional fossiliferous Potsdam strata and pre-

ata of: ane Olenellus group uear Poughkeepsie, N.Y Am. Jour. Sci., 3d ser., vol. 34, 1887,

38 oF i Lower Cambrian.

Dorations in 1 the Wappinger Valley limestone of Dutchess County, N. Y., No.5. Dis-
tea Potsdam strata at ee onan N. Y. (illustrated by map, Plate vi). Am.

oe in the Wpterncor Valley iin oktonee ee other formations of Dutchess County,
Bel. 8 ad Jace Vol. 38, 1889, pp. 139-153, .

ton ©. i inty, New York, shtan chides green ‘na purple slates,

s? examined the geological structure of the mountain, stating -

cally, the rock is here very variable. It is everywhere calcareous, all its —

a1 ‘conspicuously so; from being compact and massive it changestoarock —
) thin slabs or to one ‘Eplittin g into the thinnest leaves, which are covered

1 reconnoissance in the crystaWine rock region, Dutchess, Putnam, and Westchester -

7

Coty oll

i

>

sr

a

,

A? S'S 4 Fag) “a qa ee ee Ce 4 ee ee “ —~ ng es oye o£ oe
2 7 - ro ie —— > . ts
~ re ms 5S Ne
7 na ” i vt m
1120 : THE” CAMBRIAN. ae a se
> and - F ee ion

_ description is given‘ of the slates and shales, and it is stated the forma:

- An examination of the sections and the fauna of the “ Granular Qua:

stone and calcareous shale inwetiately overlyi ing the Olenellus lime :
stone, at the south end of Stissing Mountain, he discovered a faut
that is correlated with the Middle Cambrian or Paradoxides ‘aan
‘thus establishing the mitidle member of the Cambrian system in addi
- tion to the Lower Cambrian and Upper Cambrian that had been pre-
viously found in this region. A plate illustrating the fauna accom m0.
panies the paper. -
In 1887 Mr. C. D. Walcott! parblighed a description of the fauna 0 of
the Upper Taconic of Emmons, of Washington County, New York. r
this a statement of the stratigraphic position of the fauna was made,
‘based on the correlation with the fauna of the Georgia slates of Ver
mont. This was followed in 1888 by an account of the discovery o
fossilsin the Granular Quartz near Bennington, Vermont.’ The discovery
was further described i in a paper which followed on the Taconic systel m
of Emmons,’ where an account is given of the mode of occurrence of
the ‘Granular Quartz” in western Massachusetts and Vermont. €
quartzite is referred tothe Middle (now Lower) Cambrian zone, of which
the Olenellus bearing shales of the Georgia section are the type. 4 A

tions of the Upper Taconic have a thickness of 14,000 feet. In these
the Olenellus fauna occurs more or less abundantly at various horize ns
_ and “Taconic” shales and slates, shows that the former is stratigraphicall
and faunally the equivalent of the upper part of the latter; while ’ tl
“Granular Quartz” is a sandy depositof the shore line, and the shalesiait n
slates the offshore accumulation of sediments. On the map accom
panying this paper the geographic distribution of the “Granular Quart Zs
the * Red sandrock” of Vermont, and the Georgia slates and their south cL
ward extension as the Taconic slates is represented. — ; 5 :

In a tabular view of the American Classification and Nomenclature
published in 1888, by Prof. Jules Marcou,° the Taconic system is divide
into upper, middle, and lower divisions. In the upper division t
Potsdam sandstone, Swanton slates, Phillipsburg and Point Levis‘ or
mations are included. The middle division includes the Georgia i
mation and the St. John or Paradoxides zone, of New faker
_ Braintree, Massachusetts, and of St. Mary’s Bay, Newfoundland. —
the lower division are the Chuar and Grand Caton formations of th
Grand Cafion, Arizona, the sandstones of Great Bell Island, and th
slates of St. John’s, Newfoundland. The confusion in this table is x

1 Fauna of the ‘‘Upper Taconic” of E1nmons, in be Sp esa County, New York. Am. Jour.§ 3 3
ser., vol. 34, 1887, pp. 187-199. agi 4

2 Discovery of fossils in the Lower Taconic of Emmons. Am. Assoc., Proc., vol. 36, 1888, pp. 212, 21

3 The Taconic System of Emmons and the use of the name Taconic in geologic nomenclature, ; : An
Jour. Sci., 3d series, vol. 35, 1888, pp, 229-242, 307-327, 394-401.

4Op. cit., pp. 241, 242. :
. > American Geologica Classification and Nomenclature. Cambridge, 1888, p. 79. SS

Pe.
‘ a Tt te 7

q ne ~ 1 ¥

* 3 “ na com r.

7 / : ~~ g

kgs POTSDAM SANDSTONE 113

othe. of the 1885 paper. The Swanton slates, of Hudsen
¢ Phillipsburgh and Point Levis formation of Calciferous
ire . laced with the Potsdam sandstone; while in the Lower Ta-
Ww re e find the sandstones of Great Bell Island. which are the geo-
livalent of the Potsdam sandstone.
¢ the summer of 1888 Mr. ©. D. Walcott visited Newfoundland
1d* a section on Manuel’s Brook, Conception Bay, that extends
e Archean gneiss up to the Olenellus and Paradoxides zones.
mbroken section it was found that the Olenellus fauna occurred
i thse and the Paradoxides fauna above. This necessitated a
on of the classification of the Cambrian. The Lower Cambrian
e Olenellus fauna is at the base; next the Middle Cambrian
EiParsdoxides fauna, and lastly Oey Upper Cambrian or Potsdam
it the summit of which the Dikellocephalus fauna occurs. This
age the “Red Sandrock” series, the Georgia shale and
the “ Granular Quartz,” and the “‘ Upper Taconic” of Em-
neath the Middle Cambrian or Paradoxides zone of the Atlantic

tad

a paper on the fauna of the Glenellus zone? a brief historical re-
he en of the rocks referred to the Olenellus zone in Vermont
_ mn New York, and also an account of the sections and the dis-
n of the fauna.

; ap read before the Geological Society of America, December
Dr J. E. Wolff noted the discovery of fossils of supposed
Cc imbrian age in the limestones of the East Rutland Valley, Ver-
The limestones rest conformably upon the basal quartzite car-
e Olenellus fauna.*

lam sandstone.—The Potsdam sandstone of the Adirondack area
rs only in a few small outcrops in Vermont and eastern New York.
fding to Prof. C. H. Hitchcock, there are three different localities
mont:* near the Lake Champlain shore in West Haven, Orwell,

s east part of Shoreham, in the counties of Addison and Rutland.
iitans of these of suificient importauce to be indicated on the
. The outcrops in eastern New York are practically a con-
ion of the Vermont exposures. They oceur in the vicinity of
!, New York, and south to Fort Ann, Washington County.
€ review of the references made to the “ Red Sandrock ” series
n nt, frequent mention has been made of its correlation with the
2 Sandstone as well as of the correlation of the “Granular
(7 with the Potsdam sandstone of the ‘Adirondackarea. As now
hese two belong to distinct geological liorizons, as claimed by

iokteat - aeietines ietth adnate aed omen RT ORR eer ee ———

> v7
J ‘

al succession of the Cambrian faunas of North America. Nature, vol. 38, 1888, p.

= a _ : ——
tt, C .D. The fauna of the Lower Cambrian or Olenellus zone. 10th Aun. Rep. U.S. Geolog-
J, 1890, pp. 509-763.
ae Soe. America, Vol. 2, 1891, pp. 334-337.
Bull. Paleozoic rocks. Report on the geology of Vermont, vol. 1, 1861, p. 265.
81——_8

-*

ae

te

Ca Oe |

: Saye, Emmons in 1842, As the = Et Potsdam pandatoat in ‘this.

‘a limestone of the En glish geologists.

rs stone.’ He subsequently correlated the sandstones that are extensive ve

from the Georgia slate and ‘Red Sandrock,” is spoken of in the de-

the Upper Bano This is the same horizon referred to on page F

trict is an extension of the sandstone of the Adirondack sub- -area wit
its borders, the review of its literature will be united with that. of che
typical Potsdam of the Adirondack district.

The occurrence of the Upper Cambrian or Potsdam ZONe as distinet et
scription of the section crossing the town of Georgia, Vermont,’ whe re
mention is made of the discovery of a fauna closely related to that @

pi 14, .
' In a description of a section crossing the typical Taconic area « :

tare New York and western Massachusetts by Mr. C. D. Walcott

the typical Potedam sandstone i is not recognized. It is stated that e¢ a

CANADIAN EXTENSION.

The Canadian extension of the Northern Appalachian District is fron D
the United States boundary northeast to the vicinity of Point Levi
Quebec, on the western side of the extension of the Green Mountain 6
Sutton Mountain anticlinal, and from Be peta down the south shor ea

boundary, are also inekided

The first notice of the rocks, subsequently referred to the Cambr a
in the vicinity of Quebec, was by Dr. J. J. Bigsby. He divided tl
strata into three series. First, the slaty series, composed of slates an
Breton presto passing into a brown limestone, and altey

with fisalla sdeaar the limestone ‘ series; third, gneiss. In the 1 bed
of this eoniiailenats on the south side of the. St. Lawrence he noti ce
the presence of trilobites, encrinites, corallines, and other fossils. | a
considered them above the supposed equivalent of the Carbonife ou

ie
In his description of the succession of the strata at Montmore
Falls, Dr. E. Emmous states that the rock forming the falls is a gneit
and in the figure illustrating the section the Potsdam sandstone is sho
resting unconformably upon the gneiss and subjacent to the ‘Trex
limestone, but with a.conglomerate between it and the Trenton im

1 Walcott, C.D. Second contribution to the studies of the Cambri ian Reusine of North America, U
Geol. Survey, Bull. No. 30, 1886, p. 19. = oe
-?The ‘Laconic System of Emmons and the use of the name Taconic in Geologic nomenclature. 4
Jour. Sci., 3d ser., vol. 35, 1888, p. 240. ~ 6} ‘s
3On the acaliiey of Quebec and vicinity. Proc. Geol. Soc., London, vol, 1, 1827, p. 81. 35% oe
4Geology of the Montmorenci. The American Magazine, vol. 1, ae4l, Pp 148, ‘

Be

:
ms .

“; ‘ +. ae 343 F
~ “se . , =!
‘ - “ - _ A => tat, cae . iM + ty
~ 2 7 - a J ~ ~
“ ASL ; : a>. ROE Pepe ‘cn :
‘ ad = ~ - a

es . .
25 re «OS. al ww é ; *

.; Ps Fin at 9 Dy = i» —-
‘ j : :

pears \NADIAN “BXTENSION. coer, oF 44h eee

«aR ay
¢ Sar el

ive
Ny
Ao x
. Se
*
ik

ion of. buildings, both publie ana private, and in
3 sec ction of Jefferson County, comp York.? These nesimahey

t a ist followed the correlation ada Ss Dr. Emmons, aa fi red
to the Lorraine — or Hudson River group.

ne One Rosier ; and they are ne ihiee described in ‘dies report for
ris is is yea in the peer for 1847—48° by a Ase eae of the rocks

the west which are now supposed to be of Ginbene age. They

then referred to the Hudson River group, with the possible addi-

hat these recognized rocks of the Hudson River group have a con-
i ae run from Lake Champlain along the south bank of the St.

Ww ance to Cape Rosier.

¥ bof progress for 1849-50, °a preliminary cunt is given of
| of rock met with. They include the dark gray slates, gray,
and occasionally red shales, hard sandstones, and a me and green

r Wr n iors, and now, in part, to the Cambrian by Dr. R. “W. Elis.

a report for 185253 6 a description is given of the strata on the north

ga ' says that it would be hazardous to pronounce with confi-
what it is, from the probably contorted condition of the strata. In

a t °), no folds have been detected. They are thought to be about

at jin thickness. This is the first preliminary description of the
as and shales that were subsequently referred to the Lauzon

"y Series of the Quebec group.’

ew York, part 2, Gatiehiains the survey of the 2d geological (northern) district. 1842,

a + “

the generalstructureof an extended area in North America.] Geological survey Canada,
gress for 1843. 1845, pp. 6-13 [Documentary Edition.]}
,E. Geological survey Canada, report for progress 1847-48. 1849, pp. 2-17 [Documen-

-

Ke |Report on rocks on south side of the St. Lawrence.] Geological survey Canada
B3 a 1849-’50. . Toronto, 1850, pp. 32-33.

Fe” loration on the north side of the St. Lawrence, between Montreal and Cape
Geological survey Canada, report ef progress for 1852-53, 1854, pp. 5-74.

tetione of Quebec, with the gray sandstone terminating the |

,as seen Pinky Cape Chat toward Cape Rosier, going down the river.

ao
on of the Shawangunk conglomerate. In their extension it is stated4

e sandstones, however (supposed torepresent the Oneidacon-

RE ee ee Nea oe Saw re Ue nn eae
4 Tey 7% ~~ “a -

or 2 of the St. Lawrence between ay Bene River ard Quebec. At_

Bel et

~

be, ae 7
:

> the St, Lawrence, near Point Levis, the rocks are stated to be formed of

~

id 7 = ey Re «oes Bee Re Ss Os ea rere tae fry ee a dope
DRESS oe Sal OTL OLR Ne
2 4 ES Ot ey ‘ of aaa a aS ay me Shs ag es

on = ~ A ‘ ~ Pre --

“16 whe “THE CAMBRIAN. Ps ee

nada at Point Levis during the years 185657, Mr. E, Billings, paleon-

Dr. J.J: Bigsby, in describing the geology of Quebec aa ae ens
virons, states that the Potsdam sandstone only occurs distinetly, : as f
-as yet known in the neighborhood, at the Falls of Montmorenci ; “but ;
at Jeune Lorette there are traces of it. He says that— . a.

The sandstone of Montmorenci has been unhesitatingly declared to Sopisacae the 4
Potsdam rock by the New York State geologists, as well as by Sir Charles Lyell and
Mr. Logan. With these high authorities I have only to concur. Its geological posi-§
‘tion is that of the Potsdam sandstone ; but its aspect and mineral condition are very
_ different from that of Lake Superior aul of the Thousand Islands, near Kingston, “4
Upper Canada.? |

In describing the geology of the Falls of Montmorenci, he says:

The sandstone is plentiful on the east bank of the river above the bridge, and is 2 .
yard or more thick, as well as on the west bank both above and below the bridge; —
the plane of contact with the enclosing rock being clean and abrupt. It is white, |
brownish red or bright green, in well defined layers. Bowlders of the gneiss occur —
init. = a

A section is pairaduced in which the Potsdam sandstone is repre-
sented as beneath the Trenton limestone, and with the latter resting
unconformably against the gneiss. It is stated that the Potsdam sand- 4
stone at this place has not yet been found to contain organic remains, | 4

Dr. Bigsby described the north shore of the St. Lawrence, from Quebec —
to Cap Rouge, as consisting of frequent alternations of gritty gra) y
sandstone, and red, brown, and black clay shale. On the south side of f

minute alternations of clay-slate, coarse sandstone, calcareous and other!
conglomerates that were met with on the north side of the river.4 i
In the report of progress for 1852-53, publisued in 1854, Sir W. E
Logan® describes the red and green shales and green anndstonea from
Cap Rouge to Quebec, considering them to belong to the Hudson Rive
group of the New York section.
In a description of the Silurian rocks of the environs . of Quebee, the
same writer ® states that the only exposure of the Potsdam formation i nm
the vicinity of Quebec is at Lorette, where the sandstone is 7 metresi in
. thickness and without the fossils which characterize the formation i in
other parts of Canada. The shales and sandstone of the Sillery forma-
tion are stated to correspond to the conglomerates of the Oneida oa
“mation of the New York geologists. This same view was expressed i in
the geological essay prepared for the Paris Exposition of 1855 | by
Messrs. Logan and Hunt.
- From the collections of fossils made by the Geological preety of Oat

10n the geology of Quebec and its environs. Quart. ‘Jour. Geol. Soc., vol. 9, 1853, pp. 82-101. ; ae
_ Op. cit., p. 84. 3Op. cit., p. 88. -4Op. cit., pp. 94,95.
§(Exploration on the north side of the St. Lawrence, bevween Montreal and Cape Lourment >)
"Geol! Surv. Canada, report progress for 1852-53, 1854, pp. 33, 34. ‘
6(Sur la formation silurique des environs de Québec.) Soc. géol. France, Bull., 2° sér., v6l 12,
p-505, - ‘ art ; oo *

LA
* b

- 3 . ~ 6 nae A ws a 7 + a a < a =. aa » wil % ~ 7 -»!
is Ree ae eae re. NS SG Ft ge he TE ee
OR I, ae Le ke ; ae a eens hs =a

+ a all a pa s ~ : X nf S
espe ced A Jeet | :
5 een OF 4
= eo : _ CANADIAN EXTENSION, : 7
<— survey, decided that the rocks there and those whichhad =”

ssociat ated with them by Sir William E. Logan belonged at the
of ti f the ees Silurian and not at the summit, as had hitherto been
. - These conclusions were announced by Logan in a letter to Mons.
sar rrande published in 1860.! In this letter the whole Quebec group,
om n the base of the magnesian conglomerate with their accompanying
nes sian shales, to the summit of the Sillery sandstone, is stated to
have a thickness of perhaps from five to seven thousand feet. It ap-
. pear S rs to be a great development of strata at about the horizon of the
| y and Calciferous of the New York section. .
_ He says he is not prepared to state that a typical form of the Pots-
ise mn n sandstone i is present where the shales are in greatest force.

ae either amI prepared to assert its absence, as there are in some places masses of
ranula quartzite, not far removed from the magnesian rocks of the Quebee group,
Lich require farther investigation; but, from finding wind-mark and ripple-mark
oe succeeding layers of the Potsdam sandstone where it rests immediately
a the Laurentian series, we know that this arenaceous portion of the formation
t have been deposited immediately contiguous to the coast of the ancient Silurian —
f a prtiere part of it was even exposed at theebb of tide. Out in deep water the de-
r tay have been a black, partially calcareous mud, such as would give the shales
: boatines which come from beneath the Quebec group.
Canada no fossils have yet been found in these shales, but the shales resemble.
1 which Oleni have been found in Georgia (¥ermonty. These shales appear to
posed between eastward dipping rocks equivalent to the magnesian strata of
) nebec group, and they may be bronght up by an overlapping anticlinal or dis-.
cat: ic on. We are thus led to believe that these shales and limestones, which may be
ubord linate to the Potsdam i incaivaniens will represent the true Primordial zone in
prada a >
i n 1863 Sir Wm. E. Logan published his great résumé of the work
on ne by the Geological Survey of Canada from its commencement to
5 _ He describes the northward extension of the Georgia series
l a Sandrock of Vermont into Canada, stating that they had been
ad eat a short distance when they become faulted out and replaced
ter formation.‘
ne Siler shales eae sandstones, as well as the conglomerate beds

fo

n of the Calciferous-Chazy formations of the New York section. :
BV s and Sillery formations are referred to the Quebec group, and

Mountain range. The Levis formation is divided into seventeen
, Ce onsisting of alternating calcareous shales, argillaceous shales,
Nes stone conglomerate, and gray sandstone. The upper beds consist of

‘ =e. ‘Remarks on the fauna of the Quebec group of rocks and the Primordial zone of Can-

dis n Naturalist, vol. 5. 1860, p. 475; vol. 6, 1861, pp. 106-120; Am. Jour. Sci., 2d ser., vol. 31, 1861,

Remarques sur la faune des roches du groupe de Québec et sur la zone 2 SEE du
. géol. France, Bull., 2° sér., vol. 18, 1861, pp. 309-314,
t. Sci., 2d ser., Vol. 31, p: 219.

ca perrey of Canada, Report of progress from its commencement to 1863, Montreal, 1863,

“
—<—T

é | red: and preen aisles with thin layers of gray BES or ‘quartaite tm 3

- -with a thickness of about 2,000 feet, forming the Sillery « division of the 4

below this a third division of gray limestones and limestone conglom-—
erate occurs in beds of from 1 to 6 inches thick. A species of Salter.
~ ella was observed in the limestone, and a species of Archeocyathus in

the shales. ‘The third seriesis assigned a thickness of 700 feet; and the

_ into three parts: ‘Levis or lower; Lauzon or middle ; and Sillery or up-— -
per. The Lauzon or middle division embraces the ria green, and pur-
ple slates of the section above and below Quebec and on the island of

of Lingula. The sandstones and accompanying shales of the original

of numerous graptolites and Calciferous-Chazy fossils.

_bowlders of limestone were found containing fossils of the Olenellus

_ ress for 1866, to 1869, 1870, P. 120, pes pias Oe a Some

ok ie a Bi Mil, eS EN he me os ee _ ee Sate > ee ee
Sos ERLE A Se ae eee ee AE Sai cs Le Se BIS Sirk
2 . “Fo C: = >. my 4 4 wv; J -
: me “ a Se - “3 > :

118 Ove Seer om ‘CAMBRIAN. ee raataiy See ares

. < A
oe Rioes eo

_ which Lingula and Obolella were found. Atthe summit of the red: an a
green shales, interstratified sandstones appear and succeed the shales, —

Quebec group (p. 232). Subsequently he! divided the Quebec group y

Orleans. The only fossils known were Obolella pretiosa and- fragments —

Sillery were referred to the Sillery or upper division with the exception —
of those separated to form the Lauzon. ‘The Levis, or lower division, ~
was distinguished by its yellow, dark and black cies and the Dresenaay

‘Up to this time none of the rocks of the Quebee group had peeital
referred to the Cambrian system, or to an equivalent formation sdeneath
the Calciferous zone of the New York series. Messrs. Biiineal Halle
and Barrande spoke of the Primordial character of some of the fossils
of the Point Levis conglomerate, but the series as a whole was referred:
by Mr. Logan to the Calciferous-Chazy zone. ;

Sir W. E. Logan also described the conglomerate beds of Bie Hand
bor and Trois Pistoles on the shore of the St. Lawrence River, where

fauna.? The shales in which the bowlders occur are supposed at thé”
present time to be of Upper Cambrian age. a.

The report on the south shore of the St. Lawrence River below Que: |
bec, by Mr. James Richardson, contains the information that another
series of rocks came to the surface, differing Sin those pases to the
west. He says: i

These rocks have heretofore been classed with those of the Quebée group, ha they
appear to underlie them unconformably, and being i in some places marked by fossils —
which Mr. Billings considers to be of Potsdam age, they are now placed in ‘the upper
part of the Potsdam group.® ; “a

They consist at the summit of a light drab quartz rock with intercal- |
ated beds of conglomerate holding limestone pebbles in an arenaceous -
matrix, the whole forming a series 600 feet in thickness. This is super- :
jacent to a series of gray sandstones and interstratified shales with a
thickness of 700 feet in which near the base a conglomerate occurs a

Bi;

Ee

1 Logan, a E. , Report of, for 1866, Geol. Survey Canada, report “2 progress fata 1863 to 1866, 188 B6
p. 4. :
2 Geological Survey of Wanada: report of progress from its sspieareest to 1863. Montreal,
p. 260. &
3 Report on the aoniiaes shore of the St. Hawrenoy, b bop maid ae Geol. set ‘Canada: report p

- he ahs = Sy ; 20% fers F Sgt oe =
+f = = = = * 4 _—e ——F Cees
4 a . PT. : . acy > Pane eg ee ee i ee ne i
PS. ; pate Sy e: o hs
|

: Bees nee CANADIAN EXTENSION. sae Se (119
9 000 ‘et. A niiabar of species of the Olenellus fauna
1: 1 the pebbles of the conglomerate near St. Denis Station
Gre and Trunk Railway, and also at Bic Harbor.!

1 reference by Mr. Richardson of the rocks mentioned in the pre- _
ng Paragraph to the Potsdam zone is prpoed. + to by Dr. A. R. C.

pi ‘a ng this belt from Senet very large eax of the Quebee pion
therto assigned, the larger part to the Lauzon, but in some places
5 0 to the Levis and Sillery formations. He states that on any map

m zone from the other rocks of the Silurian. The group referred
0. 2 Oy the Lower Silurian. The second is “the volcanic group,
bly Lower Cambrian.” Group No. 2 is described as consisting of
t ; variety of crystalline, suberystalline, and altered rocks, includ-
|, gray, and greenish siliceous slates and argillites, great masses
ie. paetsiee and eee eons breccias and SER etc.*

If fo il ipeit- found I should expect them to indicate a lower horizon than the Levis
nai on, probably not far removed from that of the St. John group and Atlantic
“ie oe. Nova Scotia, or r Lower Cambrian. 6

A ing of ets statics of the Volcanic group to the Cambrian
. Selwyn quotes from the paper read before the Royal seared of
rd in May, 1882, as follows :°

OF er portion of this series was designated ** the volcanic belt ” from the a880-

‘were Miotsidered to be altered eruptive and irruptive rocks, but whether
ta , forming this igneous belt are more nearly allied to the Lower Cambrian
at e@ Upper Huronian is not, fossils being absent, easily determined.

| is tte map of the Dominion of Canada geologically colored from
made by the Geological Corps from 1842 to 1882, under the
oI of Dr. Selwyn, there is quite’a broad belt of aes colored
that extends from Cape Rosier on the Gaspé Peninsula
asterly along the shores of the St. Lawrence to Point Levis, Que-
om 1 Point Levis it turns more to the south, extending. along the

os.

a ke Champlain. A narrower strip is represented as oxtcnding

observations on the Piatavaes of the Quebec group and the older crystalline rocks of
ol. Survey Canada, report of progress, 1877-’78, 1879, p. 4A. Can. Nat., new ser., vol. 9,

4Op. cit. pst 5A. 5Op. cit., p. 6A.

ew Ae PP Ora ete ieee ea ye Geet ae A ars 5a ae ~ ca
qa 2 are ais Be Sts A e eee Bey sin fas ‘S: - = ei iscs mer. = eg
pe : i oe “ang Pig ‘y' yee =e ae a Pr; ee “ “t ea, 2 is Fe a aay oe ge
- 2 > aS ~ eT gto ee SG AP hes me +
9 1 0 TS Gaerne “THE CAMBRIAN. — pots) ; é RAS BULL, 81,

™ |

_ side of the latter to Lake Memphremagog. A smaller area is colored

~ the Cambrian. All of this series, as described by Dr. Selwyn and Dr

-. In describing the Silurian rocks on a previous page * he says: the

_ rocks, but in the absence of fossils it is very uncertain whether the strats ja

fois the north end of the Archean anticlinal or pues along the easte: rT

-.Cambrian in the southeastern part of the Province of Quebec, near th ie
Maine boundary, at the northeastern corner of New Hampshire. In a
map of a part of the Province of Quebec published in 1887, the dis s-
tribution of the: Cambrian about the Sutton Mountain anticlinal,
the Archean axis, extending north from the Green . Mountains, i is given an
more in detail than in the map of 1882.

In the table of the geological formations, accompanying Mactrlabey
American Geological Railway Guide, Dr. T. S. Hunt oes the follow
ing groups in the Lower Cambrian, in descending order :* -

: Potsdam.
Sillery.
Acadian (Menevian). wi
Lower Taconie. Sa
This same nomenclature is followed in the list of the Sooke for ma-
tions of Canada on page 52. | ~

In a report on the explorations and surveys in the intenoe of 1 he
Gaspé Peninsula, Mr. A. P. Low? states that the Cambrian system 1 .
represented along the Ste. Anne River and along the east and we
flanks of Table-top Mountain, by gray and black shales, limestone
and limestone-conglomerates of the Levis formation. He says: aq

- These form but a small part of the great area of these rocks, which stretches from

Cape Rosier along the south side of the Gulf of St. Lawrence to Quebee and thenee e
through the Eastern Townships into the United States. : 4

limestones rest in places upon a pinkish or gray sandstone of no great
thickness, which is seen on the Ste. Anne and Matane Rivers and on:
_ the west side of Lake Matapedia. This sandstone is supposed to D€ e
the iowest part of the system. — a

In his surveys of the eastern portion of the Province of Quebec, Dr.
R. W. Ells ‘ included in the Cambrian the extension to the northeast ©
those rocks described as Cambrian by Dr. Selwyn. As described in t 4
reports of the Geological Survey of Canada for 1886, 1887, they consist
for the most part of hard yuartzite interstratified with mica schists and
black slates. Dr. Ells also referred the trappean rocks of Broughton t to

Ells, is unconformably overlapped by the Sillery red slates, conglom ne
ates, and sandstones. Itis not improbable that some of the s ata
referred to the Lower Cambrian may prove to belong to that system of

1 Dominion of Canada. (Geological Formations.) Macfarlane’s Am. Geol. R-R. Guide, 187 9, p. 51. ia
? Explorationsand surveys in the interior of the Gaspé Peninsula, 1883. Geol. Surv. Canada, 1882-83
1884, p.14F. i
3 Op. cit., p. 12F. aya a
4Second report on the geology of a portion of the edie of Quebec. ~ Geological peaks Canaé
new ser., vol. 3, 1889, , Pp. 1K-120K, sal

«
-

a w
= ie
. Ore : \ a

. ad o ~

‘

aan 38 v oe > : . ‘ SZ
Spies Ge eg Sy one TS ’ : <
bot ADs

ee : _ CANADIAN EXTENSION. PO sy 3
= ~

ation Bhostht be yeferred to the Cambrian or to some
. ia mbrian series of rocks. In a review of Dr. Ells’s work by
C.L ). Walcott! itis suggested that from the occurrence of Lower
n sta iD fossils (the Olenellus fauna) in grayish limestone interbedded
ith» ‘purple, green, and black slates, in Washington County, New
! .. the rocks containing them occupy a similar stratigraphic position
1ose described by Dr. Ells in the Canadian section. Dr. Ells con-
idered that portions of the strata referred to the Lower Cambrian are very
uch ch like those of the gold s series of Nova Scotia, while, in part, they re-
4 le the Cambrian of New Brunswick. Stratigraphically they oceupy
pe osition between the chloritic and micaceous schists of the Archean
} d the superjacent Sillery. ?-_ ‘

The > Canadian ' extension of the rocks referred to the Cambrian System
vof. C. H. Hitchcock in New Hampshire is represented upon the
ological map of Canada, published by Sir William E. Logan in 1864 as

Q uebec group, thus being identified with the Quebec group series
n the. western side of the Gaspé limestone series. References have
en Bena. to them by various authors who have written upon the geol-
y of ‘the townships of eastern Quebec, but not in a manner to distin-
bh ‘the strata now referred to the Cambrian.
z Wi en describing this belt of rocks in 1886, Dr. R. W. Ells* states that
et. Hitchcock has referred a belt Reaied principally of blackish,
rin ec slates and schistose sandstones, which form a ridge extanding
rtheast from the vicinity of Canaan, between Hall’s and Indian
cams s to the Quebec boundary, to the Lower or Cambrian system.
ata present a well defined anticlinal structure,which is recognized,
6 adjoining townships of Emberton and Ditton in Quebec, and
a the outlet of Lake Megantic and onward to the Maine
_ The slates are penetrated by quartz veins, which in places

a3

° ana aspect the gold-bearing slates of Ditton and the area to the north-
= ost exactly resemble, as already intimated, the rocks of the Nova Scotia gold
. Bur c

S far as known no fossils have been found in this series to identify
izon, i in either New Hampshire, Canada, or Maine. This is true
of the second area inclosed on either side of the Stoke Mountains
tl ooo. anticlinal. The strata forming the western area

oe ae the aicath of Big Whale hee and in the vicinity

ey wr of Dr. .R. W. Ells’s second report on the geology of a portion of the Provinee of Quebec, —
di parte on the “‘Quebee group.” Am. Jour. Sci., 3d ser., vol. 39, 1890, p. 101-115.
R.W. Second report on the geology of a portion of the Province of Quebec. Geol. Surv.
a “1889, p. 87K.
1 bes on tl os had of a ort of the eastern townships of Quebec. Geol. Surv. Canada, 1886,

aie Ee STS Ee ID, REE CI aS BECO) Oar ar ae ee ae
xe 2 x = ; aa : ie 3 a , raed oP i. ae ae ¥.
74 ene eee - 3 or a ae at St tg ARs ay Boe tee Tt}
eg Kea eet 3 PAS | bo Ce SF eae 7
122 Rees TE CAMBRIAW. | 24 a eee
——, ~s 2 7 _ .

5 of Richmond a Bay. The abuGrvatisus upon which tiie identification is
- based were made by Dr. Robert Bell, who explored the east coast of
- Hudson Bay in 1877. He names the series the Manitounuck group, 4
correlating it with the Nipigon series north of Lake Superior. By com- —
__bining the sections of slates and sandstones he obtains a thickness “
_ 2,800 feet for the entire section on this part of the coast! - ee
ta References to the occurrence of rocks of supposed Cambrian age on
Lakes Mistassini and Mistassinis are made by Mr. A. P. Low in his
‘report on the Mistassini expedition. The limestones, owing to the 4
~ absence of any fossil remains, have been referred to the Cambrian hori-— 4
% ~ gon on account of their lithologic resemblance to Cambrian rocks a the -
east side of James Bay.’ a
A map of Lake Mistassini accompanies the report, on. which thes
boundary between the Laurentian and supposed Cambrian formations —
is traced. af oa
Dr. George M. Dawson tabulates the formations ; he refers to ‘the s
Cambrian in Ontario and Quebec as follows :4 .

3 Fe ? we

3b. Sillery and Levis.
3a. Calciferous.
’ 2c. Upper and Lower Potsdam.
2b. Keweenian.
~ 2a. Animikie.

ss SOUTHERN APPALACHIAN DISTRICT.

+ The Southern Appalachian district includes the ontoadie of strata,
: referred to formations of the Cambrian group in northern and central -
New Jersey, sontheastern and southern central Pennsylvania, weste D ;
- Maryland, Virginia, and North Carolina, eastern Tennessee, northwest-
: . ern Georgia, and northeastern Alabama. : Sa

= : ; ; Pedy

NEW JERSEY. ee
Bee In a table showing the geologic succession of the lower Secondary
or Appalachian rocks as they occur in New Jersey, Prof. Rogers *
-_ places as No. 1 of the series of formations a compact and very quart-
- gose sandstone, of light bluish gray color, approaching to white. He |
__ discovered the formation in only three orfour small isolated areas along” 7
the western outcrops of the Primary rocks. Prof. Cook refers to this
-._ -gandstone lying upon the gneiss as the ** Potsdam sandstone ” as know a

in New York. Itis only a few feet in thickness.> In asubsequent repor
- asketch is given of a section at Franklin Furnace, which shows the sand- :
:

“Report on an exploration of the east coast of Hudson’s Bay, 1877. Geol. Surv. Canada, Rep. Prog og.
for 1877-78. 1879, p. 17C.
er -- 2Report of the Mistassini Expedition, 1884-’85. Geol. and Nat, Hist. Surv. Canada, new ser, vot
ot 1885, p. 31D. > a
Ge 8 Macfarlane James: An American Geological Railway Guide. Second ed., 1890, p. a ae a
| 4 Description of the Geology of the State of New J ersey, being a final report. Philadelphia, iba 45.

5 Report of Prof. George H. Cook upon the geological surveyof New Jersey, and its progress during
_ the year 1863. 1864, P. 6, par. 9. a tains =" joe

3 EF reseci on the nck aiid passing conformably be-
, merniecent Magnesian limestone.' There are also enhagieed

Be smnérate, and the conglomerates and aiicenen of fis
= Pon d Mountain range. On the large geological map of northern

- Jersey, published in 1874,? the “Potsdam sandstone” includes
ales, 8: audstones, slaty grits, quartz rock, and the Green Pond Moun-
uglomerate ; this entire series is represented by one color,
dit ng on the trend of the Green Pond Mountain range from the
: ork oy southwesterly into the central eee of Morris

lec with the ‘« Devonian and Silurian rocks.”° This leaves the
)-€ 4 d “ Potsdam sandstone” as the only Cambrian formation within
es, The following year | reference i is eee by Prof. Cook! to the

S Near Franklin edehseg a simile unconformity occurs,
i th he same eblattidhs appear persistent along the entire northwestern

~

paper presented to the Geological Society of America December
90, Prof. Frank L. Nason stated he had found fossils of Lower
ian age in the quartzite resting on the pre-Paleozoie rocks at
roniville, Sussex County, New Jersey, and at Franklin Furnace,
same county. He also discovered fragments of a species of
na in sist Par limestone.® ;

DELAWARE,

fhe northwestern corner of the State of Delaware there is a trian-
1 ar area of sandstone referred to the “Potsdam” sandstone by Mr.
ed. d. D. Chester. He states that it extends into Pennsylvania, and is

ins limestone quarry a mass of quartzite forms what is clearly an sstiedlsra
r which i is a corresponding anticlinal of Magnesian limestone.°®
sxxtension of this sandstoné into Pennsylvania is shown upon the

-

. H. Geological Survey of New Jersey. (Map of) northern New Jersey, showing ane.
Pa as districts. 1874, in two sheets...

nf ies 1885. Trenton, 1885, pp. 53-55. ’ .

= t ad

‘elin ni I} notes on tl the pealogy of Delaware—Laurentian, Paleozoio, cae Pevtnsacve areas. Phila.
Sci. Proc, Berek 8 1806 ps 0, Agito ‘ f

ee ie ae _ ~ o tote

= vee pl oe ea Sea ee

of the highlands i in . ew Jersey, though no other actual contact

Chester Ponnty, Pennsylvania, where it occurs in the township.

of New Jersey. Newark, 1868,-p. 72. : a

4)

ek st at iE hy AN Nhe Pas Be ere ate mati. he tea
ON ei Oe aa Cae ae as caer ike eae Leas ~ ie os “I Rd. 45
arse ; sane A pier Ps t ae y ‘ ae Lo Da ESS pe 1 eR
iS, SME Mag eae eT GR “THE ‘CAMBRIA. UF, Pe sah ane ae
AL ae : ss rey Bo "PENNSYLVANIA. paw eee ise. :
px Be ie In the second annual report of the State seolieint of Pennsylvania,
- Prof. H. D. Rogers summarizes in a table the order of Stratification 3
Jee the geographical position, composition, and thickness of the lower
- Secondary formation in Pennsylvania, east of the Susquehanna River.!
a The description of formation No. I, or the peenerees of the South Moun-
tain, is as follows:, es 2 ig ,
ee se In the ascending order, the first formation which we meet with, reposing on the
primary rocks of the South Mountain, * * * isaremarkably empet and rather ae
. ‘fine-grained sandstone, usually white or of some light shade of gray. ~~ ‘They

2 formation ranges, according to my present belief, from the Delaware, at Easton, more
ee or less interruptedly across the State to the Maryland line, pursuing an undulating,
irregular belt, coinciding with the northern and northwestern side of the chain of
hills most commonly called in this State the ‘South Mountain, the prolon gation of the : 7
Highlands of New York and of the Blue Ridge of Maryland and Virginia.? %
It contains, as far as yet examined in Pennsylvania, very few organic remains, the
best defined species discovered in it being a marine plant, indicative of the Goeney CG
position into which the materials of this stratum were origiually swept. a.
I have satisfied myself that this rock is not confined to the Appalachian region of e
Pennsylvania, but that it possesses a prodigiously extensive range, not only through
Maryland and Virginia, but in a contrary direction through New Jersey and New
York, and I believe beyond those limits, constituting everywhere the lowermost for-
_ mation of the widespread Secondary strata which it encircles in a somewhat- inter- et
rupted belt, following the primary bonndary of these rocks from Tennessee to La ce
Champlain, and thence northwestward to the northern shores of Lake Huron ¢ and
_ ~ Lake Superior? .- . ee, . a

“Sl

_ Prof. Rogers recognized the sandstone at many points in N ew Jersey.
and New York, and considered it identical with the formation in north. i
oe - eastern New York, described by Prof. Haton under the name of Ca Nes
RA ciferous sandrock,‘ and states that it is probably the same ‘stratum
— which Dr. Bigsby has mentioned as existing on the north side of Lal :
Huron.’ In the table showing the order of stratification, formation, No.
ie = Tis assigned a probable thickness of 1,000 feet. a
A description is given in the third eabhens of the peopel dist
Ne bution of the sandstone as it occurs in the various comnlits of the sont a
eastern portion of the State. => — a

~~ ‘In Northampton and the eastern corner of. Lehigh the sandstone * * * is sub-
ordinate in importance to the gneiss and other primary rocks on which it rests. Se 3

iS shadinn Annual Report on the Geological Exploration of the State of Pennsyivania. ‘Harrisbur z,

: 1838, oppo. p. 19. -
oF _ . 20p. cit., p. 21. ~
= 30p. cit., pp. 22, 23. ;
4 4The Potsdam sandstone was not differentiated from the calito sandrock by Eaton. ‘He ina
me a chided the sandstone and the superjacent calcareous sandstone, under the common name of caleife ous
~~. gandrock, as one formation. + a
4p. wit, p28 6S an
3 : _ §Rogers,Henry D. Third Annual Report of the Geological nena of the State of Pennsylva nia.
>? Harrisburg, 1839, pp. 14-16. . a
om 7 Op. cit., p. 15. nies
Fe " r ‘ . .
ay, = te
nee a5 su! eh)
ae ae
st = ; “ ies So i

ee fy ss Buh . ‘ Se i Opa oe ce ae

"Soda J 5, Ps ha elas Ee ee ey ee) ARNE, ms Rn PEM
Pad > -* - . o 7? - * Cie ad |
i ape E Fa, ee . > ifoert S

Ps: cree RSA f° oho ao

In the t fourth report? formation No. 1 is spoken of as the extensive
late and sandstone formation constituting “The lowest member of our
id or Secondary or Appalachian rocks.” The slates of the Pigeon
di Is are referred to the lowest Secondary formation of the State, and
1e strata comprise different portions of formation No. I, consisting of
ark x slate and alight colored sandstone. The anuberaptiie succession
the various beds referred to formation No. I of South Mountain, south-
t of the Susquehanna, is given in detail. The intercalated Limentaiie
pedi $ considered to belong to the u pper part of the division,” and there
» bluish slate interstratified in the sandstone. In the report of the

ains from the Delaware to the Schuylkill is outlined. The white and
! ra, Y sandstone of formation I is not a continuous stratum in the belt
f the South Mountains where they traverse Northampton and Lehigh
Jor ities, but it is very probable it occurs at the base of all the primary
i idges, buried under a deep covering of loose diluvium.* Mention is

Jounty, and many details are given of the distribution of the sand-
y y rocks.

| In i his grand summary of the geology of Pennsylvania, Prof. H. D.
3 Be ers gives a synoptic description of the Primal series or “‘ Potsdam ”
nd dstone of New York, as follows :°

sin the Appalachian chain in Pennsylvania, Virginia, and Tennessee, is a thick
old group composed of two slates and two great arenaceous rocks in alternation:
he highest or Primal newer slate is a greenish and brownish talco-argillaceous

» set. (2) The next, the Primal white sandstone, i is a compact, white and yellowish,
je-grained, vitreous sandstone, often containing specks-of kaolin. This rock, which

ue Ridge of Virginia of at least 300 feet. This is the Potsdam sandstone of New
rk. (3) The Primal older slate is a brown and greenish gray sandy slate, contain-

ickr ess of this bed in the Atlantic slope in Pennsylvania is several hundred feet,
. in the Blue Ridge of Virginia i is not less than 1,200 feet. (4) The Primal con-
om erate, the lowest of the yet distinetly recognized formations of the Primal series,

sa heterogeneous conglomerate of quartzose, feldspathic, and slaty pebbles, imbed-
dina talco-siliciéus cement. The thickness of this rock in er and Tennes-

h fee York and the Northwestern States this series presents a sousteniatis different
pe, the Primal white sandstone being almost the sole representative.
4 telenese.—The thickness of the entire series is re more than 2,000 feet.

"PENNSYLVANIA, RM ae hs eee centre bo

_" ol rine year® the geographical range of the rocks of the South Moun-

jade of its various points of outcrop and its occurrence in Berks,

ton e and the mode of its occurrence in relation to the subjacent pri-—

@ Primal series, under its fullest and most diversified condition, or that which it —

sometimes very soft and shaly. In Pennsylvania it has a thickness of about -
o f easy recognition and of an immense range, has-a thickness in some parts of the

ag auch feldspathic and talcose matter. It has hitherto disclosed no fossils. The

2

. ’

— outcrops of the rocks and slates occur.

~ the anticlinals of Missouri, Arkansas and Texas, base elevate the gneissic strata o on

flags of England, and equivalent to the obolus and lingula sandstone of Sweden |

- life in the wide turbid sea.”* The paleontological record for the Prin |

-the Primal series is delineated. As a whole it extends with many in-

ion aphical Bjotetbaition, —In its ROS Ga distribution this gaeotes series. a
coextensively, or nearly so, with the other formations of the older Paleozoic ai
to be presently traced; that is to say, it shows two great continuous outcrops
stretching southwest along the Appalachian chain and the other west from the '
Lawrence, through New York, Canada West, Northern Michigan, Wisconsin, und
Minnesota beyond the Mississippi. Itis probably likewise brought to the day ir a

which it rests. a
The only fossils found were a peculiar facoid - in the newer Prima
slate, annelid borings in the Primal white sandstone, “one or ty vO
brachiopodus mollusks, especially lingula. In Wisconsin and other
northwestern localities this formation contains several species of tri
lobites, and abounds in lingule, obolus, and an orbicula.”: , Rloheg ;
were also found on Lake Champlain. | 1
Under the heading of “ Equivalents” is the following: ee - E
These strata seem to be on the horizon of the lower Festiniog group or lingula

[-
a

ac
BS
ae.

Russia. They represent, too, the primordial zone of Bohemia, and are therefore ¢ t
‘the horizon of the very dawn of discovered life.’ :

This summary of Prof. Rogers gives his information respecting. the
Primal series in Pennsylvania, Virginia, and Tennessee up to the time of
_ publication. Under the heading of ** Depositions and disturbances ol
the Primal period,” he discusses the probable conditions under whi ich
the sediments were deposited, and sums up the period as one of vast
duration ; “¢ an enormous age of quiet sedimentation with almost n

‘series is given a very few words: . Three or four fossils known. int
white sandstone, and a vaguely defined plant in the subjacent. shale
in the Appalachian region. But in Wisconsin, the white sandst x
imbeds, on a succession of thin floors, some seventeen more species.
Two of these are identical with those of the eastern outcrop, so th
total number of species known at that date was eighteen. The distril 1
_ tion of the Primal series in Pennsylvania is tabulated in volume Tha
_ local details are given in the description of the various counties in wh nicl

On an accompanying geological map the geographic distribntienin

terruptions diagonally across the southeastern portidn of the Sti
from South Mountain in Adams County to Northampton and Br
Counties, on the Delaware River.

_ Two maps of sections also aempany the neprt 23 1858. On |

at t Brey’s Run and Bioae Durham Creek to the Delaware River. 1
Attleborough, in teint County, a Shares of the. Siok sande

: 1Op. cit., Pp. 751. 2 Op. cit., p. 752. 3Op.cit., p. 781, . | “00 sit. 0.22,

ee "PENNSYLVANIA. ee eee

ies Sertanss the Erimal, slate in Berks County and repre--
the e Primal sandstone ness southeasterly from the Primal

“ees No. 4, in crossin g Lanvaster and Chester Counties, 3 passes
1 ugh the Primal series at Neversiuk Hill, near Reading, and also at
W elsh Mountain, where the Primal aunstabed is represented as Panne
a low anticlinal.

_ On | the line of section No. 5, the Primal si Sates occurs to the west _
o! ‘the Primal slates and gneiss that form Millbough Hill in Berks —
ou. nty. In Lancaster County, on the line of the same section, the
dstones occupy the south end of Welsh Mountain. In Mine ridge
Primal slates and gneiss are represented as much distorted, while
sandstone forms an anticlinal and synclinal axis.

ections Nos. 7 and 8 cross the South Mountain in Adams and York —

| mal, as stated 1 in the text. The rocks of Pigeon Hills, to the south-

3 bitheredd tad erystalline;” and the same reference is made of ie
ui fhwestern extension of the slates of the hills where crossed " sec-

samp ane ranowabat their study by Prof: 5) P. Lesley in: i8t
Ll mberland County, a diagrammatic sketch is given of a cross-section
gneiss for a long distance.’ On the following page a sketch of a
ion shows the sandstone, resting on the Azoic slates and gneiss;

id beneath ve a series of iron ore bearing slates that, in turn, are sub-

Ih i n describing the Cornwall iron mines ail some related deposits, in

and County, Pennsylvania. Am. Phil. Soc. Proc., vol. 13, 1873, p.4.
ornwall iron mine and nanse peliited deposits in Pennsylvania, Am. Inst. Mining Eng., Trans.,

ties; and the entire section of the mountain is represented as

= a a paper by the latter, on the iron ore of the South Mountain of —

the county at Carlisle, in which the “ Potsdam ” sandstone rests. on_

ni) Smee Dr. T. S. Hunt? refers Prof. se setey Primal slate of the—

~

‘-

> *

~

Pm eT. - =" > wh it Ea a . - iy F 2s ae we BA + en 28) the
ai Sty ae aN hohe nrOe es a sen nin” Ry ek Og
i 53 : bor see 4 eee tae a
| Be Rice rss 36} CAMBRIAN. | 60 Pee ae
L nas Sept k tiee As: i ee

—
CL ae

| “ophese same fieaeatanten in Potinkylvinota, Pa ae to the Lower: Tacon ictal :
bP eh, of Emmons, have also afforded an undescribed species of Lingula.! . - es, ,
-* - In reporting on the Paleozoic rocks of Lehigh and Northampton
Counties Mr. Fred. Prime, jr., states that the very lowest beds of the
xs Potsdam sandstone are actually pudding- -stones, containing pebbles the
tie size of a man’s fist and larger, aud fragments of red, unaltered ortho:
clase. The upper beds are composed of a hard, compaet quartzite con-
taining greater or less quantities of feldspar nodules. The sandstone
Ry often, as elsewhere, contains Scolithus.2. He gives the geographic dis-
4 tribution of the sandstone as found about the South Mountain in th e

gs: two counties mentioned. Of the upper Primal slates he says:

Next above the Potsdam sand stone occur hydromica slates, which Rogers has called

-' - the Upper Primal slates, but which really form a portion of the No. II limestone,
and gradually pass into this. They overlie the Potsdam vier aS and are. far
more persistent in their occurrence.® a : ;

In the limestone he found specimens of the genus Micotens tama
- Lehigh County, specimens of Lingula, and a single specimen of an

mt,
#;

orthoceratite.* In the vicinity of Allentown and Bethlehem the sand ;

stone is about 25 feet thick. The contact' between the gneiss and. the
sandstoneis distinctly seen about 2 miles from Allentown, on the behigg
Valley Railroad track. (Prof. Prime’s paper was also printed in the
‘American Journal of Science, under the following title: ‘On the Dis.
covery of Lower Silurian Fossils in Limestone Associated with Hydr 0+

mica Slates, and on other points in the Geology of Lehigh and North-
ampton counties, Hastern Pennsylvania.”)* . -#) 4

| The species of Monrocraterion was described and illustrated by. Pro f.
Prime in 1878.6 It is stated to be from the Siluro-Cambrian limestone. 3.
| Prof. Rogers referred nearly all of the strata of the South Mountain 07
- southwest of the Susquehanna River, to the Primal series. He says:
In its geological constitution this tract is without much variety, tor eg contain
Pos: scarcely any foks except those of the Primal series.” a
He describes the ridges as composed of the Primal white sandstone
and the intervening valleys and plateaus of the Primal upper slate.
._ These strata are represented as very much disturbed and extensively
_-. metamorphosed. This view is not accepted by Dr. Persifor Frazer, w 10
says that in his report of 1875 (Second Geological Survey of Pennsyl-
- \wania, CC) it is clearly shown, both in the text and in the grap iz
Atte itdainations, that the Potsdam or Primal formation of Rogers is ee
ing over all that country with the exception, perhaps, of seattere
es patches on the northwestern flank of the South Mountain chain?

1 On the history of the crystalline stratified rocks. Am. Asides Proc., vol. 25, 1876, p. 208. !

: 20n the Paleozoic rocks of Lehigh and Northampton Counties, Pennsylvania, Am. Phil. Soc. Proc,

a vol. 17, 1878, pp. 248, 249. a
3 Op. cit., p. 249. 4 Op. cit., p. 251. : Dy
a 5 Am. Jour. Sci., 3d ser., vol. 15, 1878, pp. 261-269. 7 pe
~ -—- 624 Geol. Sur., Penn., DD, 1878, pp. 79-80. ;

i 7'The eclaae. of Poanistvants. Philadelphia, 1858, vol. 1, p. 203. <

. -«-8Frazer, Persifor, jr. (On the relations of the South Mountain rocks in Pennsylvania.) “Ab
- Mining Eng., Trans., vol. 7, 1879, p. 336.

PM rat "PENNSYLVANIA, 4 HAG “429°

g the eaniery a the Martic antielinal in Lancaster County,
'razel calls attention to its exposing fundamental gneiss and gran-

Y ds in the new railroad cuttings along the left bank of the Sus-
nna River and how it sheds off to the north and to the south at
16, 096 feet of Primal ap eae ?) slates.!. In a special report

1a thickness of the quartzite above water level is not much over
= Between — pneaeurs and the sbeaonanas there is, he icing

ig as its name, to the larger part of the whole Wea but generally the

2 and the formation last described.‘ ’

s the result of his survey of the southern parts of Montgomery,
sks, and Philadelphia Counties, Mr. Chas. E. Hall’ decides that the
ath Valley Hill hydromica and chlorite slates, which were consid-
d by Prof. Rogers as equivalent to his Primal of the North Valley

srlying the limestones of No. II or the slates of the Hudson Period.
also gives a description of the Primal quartzite of Rogers, speaking
of it as the Potsdam sandstone.’ He gives his opinion of the age of
, sandstone known as the Edge Hill Rock, in Chester County, as
fc OWS : : “The Itacolumite, or Edge Hill Roek, I consider proven, be-
ond dispute, to be the equivalent of the Potadam sandstone.” 7
In a memoir upon the geology of the southeastern portion of Penn-
\ ane Dr. Persifor Brazer gives a summary of the aire charac-

ene the Primal or igre of tis The Sect dr dis-

on the Martic anticlinal and on ripple marks on a slab of limestone}. Am. Phil. Soc., Proc.,

oh cae

Seier had aiade of occurrence of the “ Chikis” quartzite. The-

ibly. growin 1 the deep more and more chloritic until this mineral lends its BR

cts series of slates intervene between the lowest rocks of all on the i oe .

r t to the quartzite, are referred to the Aavbhiak: the quartzite alone

wr ¥.

1, are not altered Primal slates, but no other than a series of slates |

—

LW

yes RE® The NEDSS or Kennett rock division, he » identifies with Mr. Hall’s 's Edge Ui ul

of a gneiss or syenite loosely compacted and laminated.” The second or |
- Kennett rock is the upper division and “it is a thin-bedded rock, lying ©

Re be the same sand formation which in northern New York underlies the Corniferous:

~

from the gneiss by nonconformity.* aia a

quartzite, and is generally large-grained.”! ae

1 Geological notes in the several townships of Chester County. Second Geol. Sarv. Pace The § i
‘ology of Chester County. C4, 1883, :p. 307.

‘Penn., CCCC; 1883, p. 159.

le TG ns SS ROS See Pn eee eee ee
are Fae me 23 ee 3 rs ‘oat a tae peor
ae Fi ies ae <i Powel pel y
130. - : _ THE CAMBRIAN. So ee
- =

Dr. ore atyidén the Potsdam sdpiiione Sorihdione ine an upper anda lowe

rock. sé : :
“The lower is the Toughkenamon division. Dr. Tinshe himself ‘says Xe
that the latter, or the lower division, “is composed of weathered particles —

in plates of fairly parallel sides, composed of fragments of white Jimpid — :
a
Prof. Lesley quotes Prof. Rogers’s description of the Primal series as
it occurs at various localities in the county, together with many of .
Dr Frazer’s observations; stating that he described three principal and —
a few very subordinate and doubtful areas of the Primal rock north of
the Chester Valley, One important conclusion of Dr. Frazer’s is here :
quoted : - re
In mentioning thus the ‘‘ Primal,” the quartzite and quartzose sandstone alone are
considered here. It will be seen further on that abundant evidence sustains the view © .
that the greater part if not all of the weathered feldspar porphyries, conglomerates, —
&c., in the townships both north and south of the Chester Valley are really Lower —
Potsdam. The effect of this would be to add a border of these rocks to the area of
the (silicious) Potsdam as at present indicated on the map, and thus contract ie
much the remaining area of real Azoic or Hypozoic.? a
The report of Mr. E. V. D’Invilliers upon the ae of the South i
Mountain belt of Berks County contains an extended description of the su
‘“‘Potsdam” sandstone, or No.1 of Rogers’s classification. The opening —
paragraph throws a doubt upon.the correlation that has been made of

this lower sandstone with the Potsdam sandstone of New York: 4

It would be safer to name this formation the Reading Sandstone ; but in the descrip- ¢
tions of its outcrops along the Little Lehigh, the Lehigh, and the Delaware Rivers >
in vol. 1 of this report, it has been called Potsdam Sandstone, taking for granted that —
any sand formation underneath the Magnesian limestones of the Great Valley must 2

[ Calciferous?], Chazy, and other limestones of the Mohawk Valley.? _ ee
The lower sandstone or conglomerate and the lower Primal slates 0 Oo! id

Rogers were not recognized in Berks County. |

The lowest bed of the sandstone, always seen resting « on the gneiss, is a coarse con-. *

glomerate of angular quartz rock fragments of all sizes in a silicous paste. * * * ;

The term sub-Potsdam conglomerate would express its position underneath the Pots: ~

dam quartzite white sandstone proper, belonging to it by conformity, and separate sd

-*

A detailed description of the outcrop of the sandstones and their
general character follows. Certain areas of slate exist in ‘slosiene be.
tween the sandstone and the Magnesian limestone and are referred to
the Primal series. Where the slate is not present the limestone is im-

2 The geology of Chester County, after the surveys of Rogers, Frazer, and Hall. Second Geol. 1 TV.

3The geology of the South Mountain Belt of Bets Seer Second Geol Sary: of Penn., 4) Sy
vol. 2, p.99. Cy res
*Op. cit. p.100. one eet ES _ =f Rae

il Ee soin System, is a estihinr formation in the middle strata of which occur
‘eldest fossils yet found in the vicinity of Philadelphia. The lower part of the
uation is the pale sandy slate which forms Edge Hill and Barren Hill, and the
rthern base of Chestnut Hill. Theslates are closely folded and stand often almost
eee * * * Asandstone, which from its great a pe gan at bs tp la

* * On top of this fossiliferous sandstone is a series of soft, iron- Veatile

hs sae E
«3 imonite).?

ito ; occurs in Lehigh and Northampton Counties. It rarely exceeds 25
in thickness, and there are no underlying rocks of any thickness

J 2 et ween it and the unconformably subjacent Laurentian rocks. The

stone.°
Prof, J. P. Lesley’s hand atlas of the sixty-seven counties of Bednar’

va nia contains a description of the rocks referred to the Potsdam
‘quartzite, No. I, of Rogers, in each of the counties in which they occur;

: ei nor “
“a ‘Prof. Lesley’s résumé was followed in 1886 by an important contri-

0 Rogica Congress for the system he places under the heading *‘Cam-

oric” the Hellam quartzite or Potsdam sandstone. The lower series —

saleose slates of Rogers are considered in all probability as identical
‘with the Azoic schists ; ; and it is stated that abundant instances occur

a iineated. The talcose schist of Rogers, or the upper uae of his
Primal series, is referred to the “Siluric” as “hydro-mica schists.”° _
aor, 1. Sterry Hunt objects to the interpretation of Prof. Rogers, that

‘MS.

eld work of the survey, from 1874 to 1884. Second Geol. Sury. Penn., X, 1885, pp. exii.
Ge: ral notes. Sketch on the geology of York County, Pennsylvania, Am. Phil. Soc., Proc., vol.

. ee “ea

o th os ; - > ae, i Fae ee We Pat eX es ~~, 7 Pe.
ent 4 ies * Bie ae Se «S Fae e * as PI Sas at ae gS
= AS \, i : : y ks

Ce oe + rae A ny sind = wa eth :

fe > + ~
5 ae fo PENNSYLVANIA, idk:

Y
s, often decomposed into variegated st carrying extensive beds of iron ore —

_ The “ Potsdam” sandstone is described by Prof. Fred. Prime, jr., as __

rimal upper slate of Rogers is classed with the Siluro-Cambrian lime-

al nd the geographic distribution is shown upon the maps of the counties, —

ation by Dr. Persifor Frazer entitled “A sketch of the Geology of —
rk County, Pennsylvania. ” In adopting the classification of the —

of f the unconformable contact of the quartzite upon the supposed equiv- -
a at schists i in Chester County. On the geological map pent ty eho:

7
ie |

>» a, i. — Re POY a Vet vs eh at ha . Re L - > es Sey =
eo = t 3 3 eae bas 4s sia Neer ate. abe ies ey
aps = . ee No es ¥ Wyse ae. Boe Pee ea BA
e , ? i a he 4 ss ae ee ee noe
aA % ; ~ Rpt RN ee a O : oe
“4 182 ne. : x THE ‘CAMBRIAN. Weommemetics tre
* ; . 4 = “ee Fee aM ¥ LS,

sieht Primal s endatbice, ‘Asivoral janchione: and Matinal shales of central _

~ Pennsylvania are represented in southeastern Pennsylvania. — ‘He criti- — :

; -_ ¢ises the correlation upon the evidence of the presence of Scolithus line 4
_- earis, stating that he has shown it to be very distinct from that found a
ce : in the Potsdam sandstone. The argument for this is given in his “ Azoic —
Rocks of Pennsylvania.”" In a later publication Dr. Hunt concludes —
that— : ~ eh 4
ay _ There is, in fact, up to this time, no evidence that the typical Potedam sandstone
* and Calciferous sandrock of northern New York exist in eastern Pennsylvania ; but
on the contrary there are many reasons for supposing that in this region, as in east- wa
ern Canada and along the eastern side of the Champlain and Hudson River Valleys, the
period of these two subdivisions of the New York system is represented by the First * a
' _ Graywacke of Eaton, the Upper Taconic of Emmons, which, as will be shown farther ao
son, is now recognized as contemporaneous with the typical ‘Peiadagn and Calciferous _
subdivisions. Rocks supposed to represent this Graywacke series are found in the
great valley of Pennsylvania, and these, together with the divisions immediately pre-

; ceding them—namely, ‘the Primitive quartz rock, the Primitive lime tock, and the. x
transition argillite—which constitute the Lower Taconic of Emmons—are, as we shall -

' endeavor to show, represented by the so-called Primal, Auroral, and Matinal of we a

- southeastern area,? a
He refers the sandstone, limestone, and shale to his pre-Cambrian =

-. Taconian system, correlating the formations with the Granular quartzite, — ts
- Granular limestone, and Transition argillite of the eastern New York | z
section. This correlation, made long before by Prof. Rogers, is sus- | .
tained by the latest observations. The “Granular quartz” of Eaton’s — -
section is known to be of Lower Cambrian age; the limestone, of the 4
~Trenton-Chazy horizon, and the argillite is referred to the Hudson ter- |
rane. If the correlation based upon hthologie characters and strati- 4

- graphic position by Messrs. Rogers and Hunt be correct, then the quartz- —
- iteof southeastern Pennsylvaniais of Cambrian age, and the limestones, _ 4
with their superjacent shales and schists, are the equivalents of eae ‘a
Trenton and tiudson terranes. : ~J

The statement that the Upper Taconic of Emmons is contemporanes

~~ ous with the typical Potsdam and Calciferous subdivisions is no longer —
> sustained, as the Upper Taconic of Emmons is mainly the Lower Cam:
— brian of the New York section.
In a discussion on the rocks of Pennsylvania and Ne ew York, Mr, a
-. D. Rand? mentions the Cambrian of Chester Valley, near Philadelphia, ;
and, as undetermined, the hydro-mica schist of the South Valley Hill. —
He states that the Potsdam really exists in between the schist and thaw
limestone, which refers the schist to the Archean. The sandstone is
very thin, but it rests upon the Laurentian shore of the ancient ocean,
which explains the differences of thickness as compared with the rocks

to the northwest.

Sd nS 2 a

1Special report on the trap dikes and Azoic rocks of southeastern Punnayle ania. Second Geol. oF
Surv. Pa., E. 1878, pp. 134-139,

2The Taconic Question in Geology. Mineral Phy siology and Phpianeelnn A senbiil series 0 is
chemical and geological essays: 1886, p. 534, eg}

3A discussion on ihe Pecks of Pennsylvania and New York. New York Acad. Sci. Trans, vol
- 1889, pp. 50, 51. iA) Ba SO as eee :

» 27 Bie Rely Se Sis tet gag Ca dek for Eee anay 8 Bro? eee Mere EO)

eer Rare ny ese ee

ee. | MARYLAND AND ‘VIRGINIA. - | AS tae ae
* - . “ “ ” -

abe bY vie sage "MARYLAND. . 3

he Rs 3 in Maryland Riferhelt to the Primal series of Rogers. Two
ormations are referred to the Primal: (1) a hard sandstone; and (2) a
sl i Dy. varying in color from gray to brownish and greenish. On ae

2

sries is indicated. ead
t VIRGINIA.

“One of the parlickt attempts to differentiate, by lithologic characters, :
the formations of the Blue Ridge of Virginia is on the map of a section —
-erossing it east of Winchester.? The Transition, or blue limestone, is |
vee presented as passing beneath the limestone shale that, in turn,dips.

*

‘beneath a gray schistose rock. This section is of interest only when 2
in \terpreted by the later sections of Prof. Rogers. ae
ert. William B. Rogers describes in the Second Report of the Prog-
‘ress of the Geological Survey of Virginia the Primal series in the
Sestzal counties of the State, or of the Great Valley, as follows:

a (No. 1.) This rock or group of rocks, which is frequently exhibited in Perera te
o. ox osures along the western side and base of the Blue Ridge, more especially in the _ )
“middle counties of the valley, is usually a compact, rather fine-grained, white or
ae y perish gray sandstone. Where resting on the declivity of the ridge it presents a
entle inclination to the northwest—while the’subjacent and more ancient strata of
he ridge, in almost every instance, dip steeply to the southeast. In Page, Rocking-
ty Augusta, and Rockbridge counties this rock forms the irregular and broken wi
anges of hills lying immediately at the foot of the main Blue Ridge, and sometimes: |
attaining an altitude little inferior to that of the principal mountain. A level region,

m times of considerable breadth, and strewed profusely with the fragments ofthis

alley limestone. * * * Talcose and micaceous matter make their appearance in
% i - * * * ‘This micaceous and talcose variety is sometimes found in the same hill |
an: Betigiog the more purely silicious rock. The latter, in nearly all the exposures’
m the Balcony Falls to Thornton’s Gap, as well as in various other places, exhibits
ue, , fucoidal and zoophytic impressions on the surfaces of bedding, together with
Sierabis markings at right angles to the stratification, abebmtink in straight
es to great depths in the rock, and from their frequency and parallelism deter-
ing its cleavage in nearly vertical planes. These markings are of a flattened,
ave form, from one-eighth to one-tenth of an inch broad, giving the surface of

» fractured rock a ribbed appearance, and resembling perforations made in sand
Sch have been subsequently filled up without destroying the distinctness of the
ginal i impression. Precisely similar markings are found in great abundance inthe -
white compact sandstone occurring at a higher point in the series, associated with

nu ime rous unequivocal i Sereneone of fucoides.

f rst Report of 2 State Agricultural Chemist of Maryland. Annapolis, 1860, pp. 34, 35.

te, in Virgins including the gol region. Geol. Soc. Penn., Trans., vol. 1, 1835, map, oppo.

STA ef. KA > RS on ee oe; ack: he ei Be? 2
i fumetatiten cy ase oie fae AT io ee ae ia ete
oO Se ea “THE, ‘CAMBRIAN, — SEE aa

“The description of formation No. I in the third annual report 18 ¢ ve
~ follows: | : a

Sie ; 4
. = The lowest of the Appalachian rocks consist for the most part of a close-grained | fens
aya white or light gray sandstone, in some places containing beds of a rather coarse con 7
- glomerate of white silicious pebbles. Near the bottom in many instances a brown- <i
“ish slaty sandstone occurs alternating with the former, while towards the top or ]

_ approaching the next formation, the sandstone passes into reddish and brownish —
and olive-colored argillaceous slates.

This formation in Virginia is exclusively confined to the western slope of the

Blue Ridge and the narrow belt of rugged hills and mountains extending thence to —

~. the commencement of the valley limestone.! >=

a

Mr. B. S. Lyman states that all these beds seem to lie within the Vir. :
ginia and Pennsylvania geological formation No. I, wholly below the —
Calciferous Sandrock of No. II1.? a

On the map accompanying the reprint of the annual reports and ii
other papers on the geology of the Virginias, published in 1884, Prof ‘
Rogers has included under one color, formations I to III or the Primal, x
Auroral and Matinal series. On the large series of sections, however,
the three are differentiated and No. I or the Primal series is shown in ee

‘sections 1 to 19, and also in 89. nis a
Prof. W. M. Fontaine has added many details to the section of thes - ;
Primal series described by Prof. Rogers, at Balcony Falls in Rockbridge e
County. The sketch of the Balcony Falls nection is sUDDecana by fe
_ that of Rockfish Gap and Harper’s Ferry. a
For a further notice of the results of Prof. Fontaine’s work the reader Q]

is referred to the description of the Cambrian rocks of Virginia. =
Ina note upon the Potsdam or Primal group of Virginia, prepared for
Macfarlane’s American Geological Railway Guide, Prof. W. B. Rogers —

:: — as equivalent formations No. I of the Pennsylvania and Virginie r

a ~ surveys or Primal of the annual reports and Potsdam group. ‘The E

Tatter 3 is used in the nomenclature of the rocks of Virginia and We st 6 ,
fz Virginia. In the note explaining the Potsdam group, he says: a %

The Potsdam, or Primal group, includes in Virginia, where complete, besides the e°
Potsdam proper, the ferriferous shales next above, and the slates, shaly grits, and con-

- - glomerates, below this formation. It is exposed in varying mass and completeness”
on the western slope and in the west flanking hills of the Blue Ridge throughout —
much of its length, often, by inversion, dipping to the southeast, in seeming « con-
formity beneath the older rocks of the’ Blue Ridge, but often, also resting unconfor m=

ably upon or against them. These older rocks, comprising masses referable probaly

| _ to Huronian and Laurentian age, include also a group of highly altered beds, cor:
Baa ab sponding apparently to the copper-bearing or Keweenian series of northern Michigan, P<

ic

and perhaps to the lately described Dimetian rocks of Wales.‘ BG a7 aa gee

= Ina paper on “The Lower Silurian brown hematite beds of America,’ ae 4

1 Report of the progress of the geological survey of Virginia, for 1838 (Richmond, 1839),p.6. A re- x
print of the annual reports and other papers, on the geology of the Virginias. New York, Re. at,
_ pp. 197, 198. :

2On the Lower Silurian brown hematite beds of America. Am. Assoc., Proc., vol. 16, 1867, p. 14, “
_ . $0n the primordial strata of Virginia. Am. Jour. Sci., 3d ser., vol. 9, 1875, pp, 363-369.
; 4Rogers, W.B. Virginia and West Virginia. [Geological formastionns ] Macfarlane’s Am. Ge
BR. R, Guide, 1879, p. 181. Pas ey

of. J. Ti. Ganpbell published two. papers in 1879,! in which the
a revised description of the Silurian formation in central Virginia.

; Virginia. _In another paper he gives a definition of the ** Primordial”
as follows : £

a a

Ti fe Primordial —The great bed of ferriferous shales and sandstones skirting the

‘ published i in 1883.4 The section is formed of conglomerate at the base,
subjacent to shales, upon which the so-called Potsdam quartzite rests.
e upper member of the Primal series is the ferriferous shales. The

en by Prof. Fontaine will be used largely in the summing up of our

it ‘section for further details.

a formation) into (1) lower slates, (2) sandstone, (3) upper slate.

Fi ‘ste In the lower slates, or those geologically underneath the Potsdam sandstone
urs a red hemitite ore, sometimes in beds of considerable thickness and of ‘good
ity. - Thisis the so-called ‘specular ore ” of the Blue Ridge, and it has been quite
se pee at numerous points, notably in Py een and Bedtord Coun-

osed for a considerable distance on the Vesuvius property. * * * Third. The
© slates, however, are by far the most important from an economical standpoint,

ginia. They intervene between the Potsdam sandstone and the base of the cal-

observations will be noticed in the section on the Cambrian rocks

oe base of the Blue eo from Tennessee to the Potomac; in the upper part of

al ‘series of Prof. Rogers is described. » These were followed in 1880 |

a to the Primal series ot Rogers is that of Prof. W. M. Fonthind.

4s

e thickness of this section is given as 2,380 feet, and the data _
wledge of the Primal series in Virginia. The reader is referred i :

sid n an article upon the iron ores of the valley of Virginia, Mr. Andrew
McCreath divides the ‘‘ Primal or Potsdam sandstone” (Primal or Pots- |

,, invariably ald. short. In Rockbridge ees a bed of it fully ten feet thick is

| rous limestone, and they are found all along the western slope of the Blue Ridge—~

g geologically coextensive with at _ They are generally more or less disintegrated,

asen formation central Virginia. Am. Jour. Sci., 3d ser., vol. 18, 1879, pp. 16-29. Geology of
; Balcony Falls; The Blue Ridge and its geological connections. Some theoretical consider-
Tbid., pp. 435-445.
ilurian formation in central Virginia (revised). ‘The Virginias, vol. 1, 1880, pp. 41-45, 54-56.
mineral resources and advantages of the country adjacent to the James river and Kanawha
and ‘the Buchanan and Clifton Forge Railway. ‘The Virginias, vol. 1, 1880, p. 3.
tes or the mineral deposits at certain localities on the western part of the Blue Ridge. _ The
‘ias, vol. 4, 1883, pp. 21, 22, 49-44,

iron ores of the valley of mene. Am. ‘act! Mining, Eng., Trans., vol. 12, 1884, pp. 18-- 20.

ee

nd. -

¥

wre

-.

yy

g

» ne ie a a a ~y =f =, I Sew Sp one ou * bess Rea Ge ie OAR ROr 2 Lp) EAs oi JS as & ‘
; : / . tx Pe re e 7 $ qa o * sotet nes ihe. gene 7 4 :
ABB ORE are aaa CAMBRIAN. oS oe

~ modified view,” Prof. Campbell corrects the statement made in a former.

_ spanned by a grand arch, or series of arches, of Cambrian age, upturned perhaps at

_ Sometimes some partially decayed feldspathic matter occurs with the pebblea. « A . §

nae the sheet of sections accompanying “The Virginias” by Prof. wil. 5
liam B. Rogers, printed in 1884, section 9 crosses the Primal series of
Rockbridge County, about 30 iiea north of Balcony Falls. On the |
eastern slope of the Blue Ridge a small synclinal basin of the Primal
series is represented as resting in a hollow in the gneiss; on the western. 4
slope, the Primary series is shown as it occurs in numerous ‘sections —
crossing the Great Valley and the Blue Ridge. The editor of the sec ‘
tions, Mr. Jed. Hotchkiss, states in the note accompanying them that the Ni
sections are ‘‘exact reproductions, in so far as the geology is. concerned, —
of the sections as Prof. Rogers left them.” From this it is evident that ,
Prof. Rogers became aware of the presence of the Primal series on the —
upper eastern slope of the Blue Ridge in Rockbridge County after the
publication of the third annual report in 1839, as he stated then that
the Primal rocks were confined to the western side of the ridge. -
Messrs. J. L. and H. D. Campbell, while studying the geological re-
lations of the Snowdon slate quarries in Amherst County, on the borders 4
of the counties of Rockbridge and Bedford, discovered the presence of
the Balcony Falls series of Cambrian rocks and found that the quartzite
passed beneath the slate of the quarries.' On the map accompanyin 5
the paper (p. 170), an ideal section shows the shales and conglomerates —
resting on the gneiss beneath the sandstone, which they have referred
to the Potsdam owing to its carrying Scolithus borings, and above the
latter is the slate belt, in which the quarries are located. Under t aes
title of “‘ Geology of the Blue Ridge near Balcony Falls, Virginia; a

paper, in the American Journal of Science in 1879, that the rocks of tha! og
‘southeast slope are of Archean age. He adds a sentence as follows : re

We may conclude, therefore, that this portion of the Blue Ridge has been formed : :

the time of their upheaval—the broken fragments of which have been carried away
and only the abutments left to tell the story of a great catastrophe.?

Ia letter on relation of Archean and associated formations in n Vir. r
ginia, Prof. W. M. Fontaine states that he finds in Virginia a-valuable
guide to the true base of the Potsdam in the conglomerates. ; 4 4

The lowest conglomerate is not always seen. It is often very coarse, with polly 3
sometimes 4 to 5 inches in diameter,and composed of Laurentian or Huronian ma
terial, according to the nature of the underlying rock. The matrix is often shaly 0 or
slaty. ee
'. It is the conglomerates overlying this stratum that afford the best guide, for the
may always be seen. a ;

They are simply pebble beds in the slate or shale. The pebbles are from the sine 2
of a musket bullet down, and usually of quartz, often pink in ‘color. The pebbles
look as if they had been scattered over a muddy bottom, forming a very pecul jar
conglomerate in which all the material except the pebbles is a fine slate or shale,

_ ' The Snowdon slate quarries. The Virginias, vol. 5, 1884, pp. 162, 163.
_ *Geology of the Blue Ridge near Balcony Falls, Virginia; a modified view. Am. Jour. Sei. 3d set ;
1884, vol. 28, pp. 222, 223, ¢

~

6 ssumé of the section is given as it aust on the northwestern slope

roe ks. as found upon the southeastern slope. On the eastern slope the
‘str rata lie in a basin of Archean rocks forming a synclinal, a section of

‘ am
.

‘otsdam group” of the western slope. A map and figure of the sec-
n accompany the paper.2 In a second article in connection with his

erable detail,*? and mention is made of the discovery of another area

z rot, Pi Ey ee erin identifies the Gannrign rocks, crossing Mont-
mery, Pulaski, and Wythe Counties, as the Lower Knox shales and

Here are placed the Lower Knox shales and the Potsdam. The former are prob-

ably equivalent to the ogee schists of ph cea mga and the lower part of the

is coor were observed in the ube: or the Potsdam shale with the

Ro

bions referred to the Cambrian is shown on a map accompanying
paper. Further reference will be made a0 Prof. Stevenson’s paper

In a paper read before the Geological ae of America December

31, 180 by Messrs. I. R. Geiger prises Arthur Keith, it is stated that

{ They present a number of sections showing the stratigraph ic
on of the beds. In these the normal succession is limestone,

setter ¢ on n relations of Archean and associated formations in Virginia.) Geol. Chester Co., Pa.,
pol . Surv., C4, 1883, p. XV.

Le Potsdam group east of the Blue Ridge at Balcony Falls, Virginia. Am Jour. Sci., 3d ser.,
view Pee William B. Rogers’s Geology of the ea ee Am. Jour. Sci., 3d ser., vol. 30, 1885, pp.

368. ,
erat reconnaissance of Bland, erg pete and apie of Pulaski and Montgomery

of the Blue Ridge at Balcony Falls for the purpose of comparing the ;
ch practically reduplicates the lower portion of a section of the —

her, the Cambrian-Primordial (No. 1 of Rogers) is described in con- —

erred to the “ Potsdam group ” rae the eastern slope uf the Blue

tl @ Potsdam of the Tennessee section. Under the title ‘‘ Cambrian” :

exception of-Scolithus linearis. The geographic distribution of the for-.

“A

les, and sandstone. The shales succeed the limestones, and overlap _

©

rs
Rf

-
! ~

~

+) 138 eee 3 peat es “THE CAMBRIAN. oe - ee mais

3 upon the pre- Paleozoic eke the (eines in Gaia resting. upon th the —
Shales. This makes the limestones represent the Great Valley li ne
__ stone of Virginia or the Calciferous- Chazy-Trenton belt; the shales, the

- series of gray, drab, and mottled argillaceous slates and shales. This succession of

eo Re

taecd
= ho

_ Hudson series, and the sandstone, the Medina series of me New Yor ic
~ gection.! :
iINORTH CAROLINA,

_ As now known the Cambrian rocks of North Carolina are confined tz
e extreme western boundary, where the Ocoee conglomerate and
‘Chilhowee sandstone series extend across from Tennessee. This was
recognized by Prof. J. M. Safford in his work in Tennessee ; and Prof. -
W. C. Kerr notes the occurrence of thin-bedded, siliceous taken at Paint 4
- Rock, on the State line. He says of them: i

They are called by Prof. Safford, the geologist of the State of Tonnveee Chil-
_ howee sandstones, and are set down conjecturally by several eminent geologists ¢
Potsdam sandstone, They have never yielded any fossils by which their geological i
horizon might be determined. A few very thin beds of argillaceous slate are found
interpolated here and there between the quartzose strata. a x

Passing up the deep gorge which the river has excavated, the quartzites are soon —
found to be interbedded with and are finally replaced by silks and grits, the latter of
generally fine, but occasionally approaching in appearance a breccia or conglomerate 2.
These are succeeded by heavy beds of argillaceous slates and shales, which in torn :
_ give place, at Warm Springs, to a heavy bedded blue and gray limestone. This i is
- followed by a calcareous, compact, fine-grained sandstone, which presently passes
into a gray, much jointed quartzite rising in vertical cliffs along the river for 2 mil 03;
and succeeded by a well characterized coarse conglomerate with bluish gray slates
and shales, at and below the mouth of Laurel River. A little above this point comes i
in a very extensive and conspicuous bed of feldspathic quartzite, or petrosilex, which
continues for more than a mile, and then graduates through a gneissoid rock into a

eae
~~

quartzites, grits, shale, limestone, and conglomerate occupies in direct cross socio! ‘¢
a space of more than 10 miles. I have elsewhere referred to the identity of this for
mation with that which is so conspicuous on Valley River, and shall therefore call it bo
_ the Cherokee Slates. They pass in a northeast course up the Laurel Valley and
ff:

through the Smoky or Unaka Mountains into Tennessee, - ; =>
a ase

In a note on the occurrence of metamorphic Silurian rocks in North —
Carolina, Prof. F. H. Bradley states that the rocks about Franklin ar ©
of Lower Silurian age, and the marbles of Murphy and_-vicinity are th eo
paauiraicnts of the Knox limestones of Tennessee, which are of Quebec
group age.’ This statement of Prof. Bradley’s is noted here, as it is 1s
probable that the formations examined by him are equivalent to those
exposed on the French Broad, between Warm Springs, North Carolina,
and Paint Rock. If so, they may be of Cambrian age. In a paper pul DF
lished the following year, Prof. Bradley refers‘ to the strata in the
vicinity of Murphy, in southwestern North Oarolina, and takes the viev v

1 Bull. Geol. Soc. America, vol. 2, 1891, pp. 155-163. - min lag at : ¥ Er a
2 Report of the State Geologist of North Carolina. Raleigh, 1869, p. 29. oe
_ 8 Note on the occurrence of metamorphic Silurian rocks in North Carolina. Am. FORE, Sci., sds ‘Be se

_ vol. 8, 1874, p. 390.
* On the Silurian age of the southern Appalachians. Am. Jour. Sci,, 3d 8 ser., vol. 9, 1815 PP- 598 = -

vs eaten ENON ACLU Sagi Ey TO RY Me ee Spe oy pe ae ee
S Sie = Soe ay Be a ee 4 . rah fa Sau Soh x ae me oe
es “ a xr -_ ®, rs on 3 P- + a" +» ee ve
TP ENNESS | 189:
xs rs : 5 = F
Wear fs oe oa eae Say
ae Koad a Pe. « ee aah ea
i . ° 4 a
a a males is

ine ¢ whe Rléeadscs River; so much so that fareetd of the recognized *
owee strata I think is would be very hazardous to state that the

brian is represented in southwestern North Carolina. Iu his de-

tion of the stratified rocks, Prof. Kerr states that so far as known

> Pr rimordial i is represented only in its lowest member, where it crosses

a

, no! rth west border i in a few noes along the eee Mountain." oa

ae pe aa

‘

$s he :) Sadafieation adopted by Dr. Gerard Troost, in his fourth reheat
o ae of the State of Tennessee, is as follows :*

1. Primordial, or Primitive, or Crystalline.
2. Transition or Fragmentary. ~
3. Secondary or Sedimentary.

i In mentioning this classification he says:

App: ulachian Chain. The line of contact of the Primordial rocks with
, ‘Transition or Fragmentary coincides in a general way, but not.
etly with the boundary line between Tennessee and North Carolina.

de country lying between the Great Smoky Mountains and the Cumberland
oun ag or East ce agian is for the most part composed of strata of grauwacke,

ra ely found ; sas strata are highly inclined, approaching ee some places
rds the elie; dipping more or less towards southeast and running nearly
lel with the Smoky Mountain ridge; they are covered in several places by
ntal strata of limestone of a dark gray, approaching to a black color, and hav-
‘granular structure. It is in some places characterized by Maclurites, be Sueur,
lubularia, nobis, Isotellus, Dekay, and several species of Calamopora, Goldf.4

alline series is colored blue, and the Secondary or Grauwacke

ole > a SF Raport of the geological survey of North Carolina, vol.1, 1875, p.115. Raleigh.
«2 Op. cit., p. 140.

aR fourth report of the geologist of the State ot Tennessee. Nashville, 1838, p: 630.

patie si inch on the ane of Tennessee. Nashville, 1840, p. 5.

<

s . -
fis, ree

bes Orystalline Primordial rocks form the hizheat part of the ~ :

4, Tertiary or Upper Secondary. ere

Bi eta tae la © ae. THE " CAMBRIAN. pes Sed a,

as — son’s *Siluria,” and also the observations of Prof. Sedgwick on the a
- Cambrian rocks of Wales. In discussing the changes of nomenclature ‘

\

and Iron Mountains; but the culminating ridge of this mountain chain ‘is mostl
. composed of the Gunspates rocks, while south of it the crystalline or Primordial rock

- great Smoky Mountain, exibadlawd in a southeastern direction through Sevier Coun iy:
Ihave not been able to trace it further to the northeast. This series seems to be

841, p.4. - ; : =

‘system, he says:

commences, as already observed, about the line which separates the State of Te

slaty rocks, containing here and there chlorite, passing into talcose slate—or i

‘Sevier County. I believe that this series commences with Star’s, Tellico, and Chil-

brian system—or, that it perh aps belongs to the Old Red peated hence tow:

BPS FEN DER Ss aS Teno ee a a ike ec

yok i J ‘
,. i ee b S ty,
—— ie? (ety . ~ x °
o* ¥ , rat
i] BR Pe Wot i+ | reas ¥ ro

series, composed of eireiee! slaty: eraneelolek: saudston) and. i
stone, which extend from the Primordial series to where they are’ os
under the Cumberland Mountains, is colored yellow, thus roughly. out t-
lining the relations of the Cambrian and _ pre- Cambrian rocks of e2 st ,
ern Tennessee. — Eee.

Before publishing the Sixth Annual Report, Dr. Troost read Murchis

made necessary in accepting the views of Messrs. Murchison and 1
Sedgwick, he says: | cata ee ae oa

After having pointed out, in my last report, the line of junction of the Primordial 1
or crystalline rocks in East Tennessee, I mentioned that the country west of the line,
which separates Tennessee from the State of North Carolina, is composed of grau-
wacke, slate, limestone, etc. All this country, according to the views of Murchise Dn
and Sedgwick, belongs to a new division, which they call the Cambrian system. _

This series of strata contains few organic remains; in fact, I have carefully exam-
ined, in this respect, the Tennessee strata and have never discovered any in thems ss

In his attempt to identify the Cambrian and Siluriansy sting
Tennessee, he included rocks in the Cambrian system that, under. the a
original definition of Sedgwick for that system in Wales, is surprising] y
correct. In describing the ani nae distribution of the Cambrian

I consider the termination of the Cambrian Rystein kot eet the west. This - a

nessee from North Carolina; and,as mentioned in my preceding reports, is also, wi t h
a few exceptions, the line of separation between the transition and primordial strata.
It runs sometimes a few miles into North Carolina; sometimes penetrates, for a fe v
miles, into Tennessee, forming the great Unica or Siiniey Mountain, Bald Moun i ;

a

are found. Y 2 a
Leaving this ridge in a north, or rather northwest direction, we have a series of it

quartzite. This series seems to be equivalent to Sedgwick’s Lower Cambrian series;
some extensive strata, mostly of brown or reddish brown, fine grained limestone
occur occasionally in this series; such a stratum is seen about 5 miles west fi
the Primordial rocks, crossing, near the Warm Springs in Buncombe County, 1 e
French Broad River. We have then a series of strata of slates and sandstone, nd
about 4 or 5 miles west of Newport a limestone stratum appears again, extending
through Cocke and Sevier counties, parallel to the above-mentioned high chain. I I
suppose the Lower Cambrian system terminates there. . ‘a

Upon the Lower Cambrian rocks follows another series. Iti is composed. of roofing
slate, glossy aluminous slate, and sandstone. A ridge of fine roofing slate cros

J
n

d
me

howee Mountains in McMinn, Monroe, and Blount counties, ranging parallel with the

equivalent to the Middle Cambrian. * * * <%
I consider, as stated above, that Bay’s Mountain forms the upper pat of the Ca =

1Sixth annual report of the ys aie survey of Tennessee, by the State geologist. Maal

3 th schon, and extends hoviheard as far as the line Sah saclnuaae this. .
iia fact, it continues into that ‘State. roe, :

s from which he obtained and identified Silurian fossils. Although,
light of our present knowledge, there were many inaccuracies in
orrelation it exhibits a comprelensive grasp of the views ex-
d by Messrs. Murchison and Sedgwick and unusual clearness in
rrelation of the groups of rocks in the two countries. : j
a sketch of the general geology of the Hiwassee copper region
J. P. Lesley describes the primary region of the Hiwassee and.
Rivers as a southern prolongation of the metamorphic rocks |
Blue Ridge, South pane aia and Highlands of the Middle and _
vern States. :

p atly resembles in every ae <a ay geological particular the range of the White
n New Hampshire. * * * They are not primary rocks, granites or por-
but the Primal and Matinal sandstones, shales, and limestones and conglom-
at the base of the older secondary series, baked, crystallized and upturned in
psed synclinal and anticlinal axes.

He d lescribes the section on the line of the Ocoee River as formed of
ghtl ly metamorphosed. conglomerate strata.

laces these rocks are a simple pea conglomerate, quartzose, and indebateatitied
ne hardest homogeneous blue and gray grits and scarcely altered.®
preceding correlation was based upon the view that the strata
referred to the pre-Cambrian Algonkian series were metamor-
| Primal and Matinal rocks, corresponding in age to the unal-
I Primal and Matinal rocks to the westward. That they might
» great group of strata beneath the Primal and ae teres to the

naissance of the State of Tennessee,” in which he classified the
tions as follows :4
ae formation I.—The mica slate group.
_IL—The Ocoee conglomerates and slates. |
I1.—The Chilhowee sandstones and shales.
IV.—The Magnesian limestone and shale group.

? Op. cit., p. 28.

a ae Oe m8, SS a Be EE re See os en eee ae fF 3, ae cae Seo ee
5 y <— eS * =e ‘er Se “i = i eae vorer or ue, eA a SS ae

_

= : ANUpAaGOES i and Iv were poterrea to the Cambrian. an
the formations above IV to the Silurian and Devonian Syatenna; Cale “
- The term Cambrian was used provisionally to unite the first two sd
| e stl bearing formations. The upper portion of formation No. IV, ort 18
limestone member, was subsequently, in 1869, referred to the Knox
. dolomite. oe
eta AN This preliminary report was followed in 1869 by the volume ‘
& Geology of Tennessee,” in which all the strata now referred to the
~ Cambrian are described in detail." A map illustrating the geograph ie
distribution of the formations in the State, and a transverse secti D
_ from the North Carolina line west, showing the stratigraphic relations )
of the formations, accompanies the volume. My a
In speaking of the age of the metamorphic rocks of eastern Tennes
see, which have been referred to by various authors as altered Silurian L
rocks, Prof. Safford says: ¢ s

- I have no reason for believing that this group within Tennessee includes t he
metamorphosed beds of any formation of more recent date than the Ocoee conglor m- :

erate and slates. A portion of the beds are certainly referable to the Ocoee group;

= the remainder, although conformable, may be older, and most likely are. * *
In the northern part of the State, at many points, the passage of the Ocoee beds into
gneiss is gradual and apparent. A considerable part, indeed, of our metamorphi¢
rocks can be, I think, thus referred to these beds. The question as to the greater 2
of other parts is not so easily settled, and must remain open for the present. I kn
_of.no sufficient reason for referring any of these pogen to the Huronian or Laurent n
series of Canada.? - “4

It will thus be seen that the line of Ascatondars Latweliee ‘sea 2 re: .
Cambrian rocks and the Cambrian rocks has not been closely defin L
in Tennessee. Itis only by comparison with the more clearly defined

~ _ Jine found in the sections of the Blue Ridge in Virginia that we are led
‘ to consider that the metamorphosed rocks belong to an Algonk ian
grou p between the Cambrian and the Archean. The studies which 2 ire
now in progress under the direction of the Geological Survey cleat ly
demonstrate this, and give as the base of the Cambrian a series of san d
stones. Where the sandstones and conglomerates are made up of th - 3
material derived from the adjacent Algonkian or Archean rocks th
will necessarily have something of the character of those rocks, and it
may be difficult in many instances to indicate the actual line of dema re-
ation, especially where the basal beds have been more or less alter red
~and dabuibed by the subsequent folding, faulting, and compressio ion
that accompanied the Appalachian uplift. :
As defined by Safford, Series II, or the Potsdam group of Tennessee By
consists of— a

1. The Ocoee conglomerate and slates.
2. The Chilhowee sandstone. aaa
3. The Knox group of shales, dolomites, and limestones. ee

£

~

: - - Geology of Tennessee. Nashville, 1869, pp. 182-226. : gs “Op. cit. 1 PP-1T%, 17 178...

3 tot the Lower Silurian, as the equivalent of the Calciferous and
‘zones of the New York section. This refers the Knox shale to
per Cambrian. Prof: Safford states that it is not easy to separate
peally the Ocoee sub-group from the Chilhowee, as they often run
ch other. The distinction between the latter and the Know is
1 more apparent. .
é Ocoee Conglomerate.—The typical section of the Ocoee conglom-
in the gorge of the Ocoee River, is described by Prof. Safford as
W S: . é : te < 4

4

) strata are well displayed, They are, in general, coarse gray Soinblanevebn
e, chlorite and clay slates repeatedly interstratified, all having a semi-metamor- —
spe act. Theslates predominate, andof these, the sien fei and light bluish gray,

} e shloritic and talcose varieties, are the most abundant. * * * The middle
art of the section presents little conglomerate, but in the upper part it abounds.
* * * The lower part of the gorge has several bands of conglomerate.?

7; if

ionally it was estimated to be more than 10,000 feet (p. 186). As shown

a map, the main portion of the Ocoee sablndeuka occurs south of
chucky River. In Johnson County, in the extreme northeastern cor-
‘of the State, it occurs as a narrow band next to the metamorphic
S South of the French Broad River, it occupies a wide belt to the
aia line. Prof. Safford says it is traly a mountain-making forma-

he recent work of the U.S. Geological Survey has shown that the

Cambrian.

Ar sumé 0 of the geology is given in a report upon the resources of
mnessee, by Mr. J. B. Killebrew,> which was prepared by Prof. Saf-
MI dd. It is a brief restatement of the character of the formations as
esc ibed i in the “Geology of Apaanennee and the eee map ac-

n ibe typical Potsdam; and the Geke the Lower Potsdam or Aca-
Sroup. He also thought that the rocks of North ver south

—-1Op.cit.,p.182. 20p. cit., p. 184.
4S Resources of Tennessee. Nashville, 1874, pp.26—46.

Le ae SE ac Sia ee GRE gta baa tg pee Une ree ht wa cies ian

we “a pS Fee .- . . . — rm

: 5 ah , : AT SADC S Aha eae ee ae
3 aa aerate "TENNESSEE, 2 ecie dee teats seem 143"
sees Seek

Fe

‘The thickness of the Ocoee formation was not determined. Provis-—

own 1 to Se ak the present time the dolomites wid limestone are os =

se conglomerate i is of Silurian age, and it is not to be included with

is

~

So

~

“

’

_ in 1883, by the expression of a somewhat similar view of the age of. the |

referred to the Cambrian group in the United States and Canada, Mr.

dam sandstone. The supposed subjacent Chilhowee sandstone an¢

_ references to the two formations were omitted, pending an investig 1

_ 2The age of the Southern Appalachians. Am. Jour. Sci., 3d ser., vol. 25, 1883, pp. 282-298. . ae

_ p. 100. Second contribution to the studies of the Cambrian faunas of North America. U. S. Geol. S

Q ot ys Pe = + he ey es
Be Sg Sein Be,
Sg cae Sek aa wee Sores ais be ilag cise. *
Se eS, Mgt ee ee EN hie a ONY Stade i «
14450 °> eS ‘THE CAMBRIAN. SN Se . 3 [pt Lal.

tion of two or three sniall patches not over 10 miles in : digmietbet « y a
description of sections from Athens and Knoxville, Tennessee, to Mur
phy, North Carolina, accompany the paper. : ae
_ The descriptive notes and conclusions of Prof. Bendiions were followed,

“Southern Appalachians by Mr. J. B. Elliott,?i in which he concluded with — 3
Bradley that the metamorphosed strata east of the unaltered Ocoee and —
other ‘“‘ Lower Silurian” rocks were frees of metamorphosed strata of
the Knoxsection. — < —
In the table of formations accompanying ~Macfarlane’s American :
~ Geological Railway Guide, Prof. J. M. Safford arranges the formations —
now referred to the Cambrian in the following descending: order: ey
3b. Knox shale.
3a. Knox sandstone.
2b. Chilhowee sandstone.
2a. Ocoee group. .
He places as equivalent formations, following Dana’s Manual, the“
Ocoee and the Acadian; the Chilhowee and the Potsdam; the Knox
sandstone and the Qnisifergan and the Knox shale and the Quebec.
This is the classification eeiscatastcl by Bradley. The Metamorphic
group, No. 1, beneath the Ocoee group, is correlated with the Archean, ;
In an attempt to assign to the proper stratigraphic horizon the rocks ©

C. D. Walcott correlated the Knox shale and sandstone with the Pots- 3

Ocoee conglomerate were referred to a position corresponding to the
horizons of the Olenellus and Paradoxides faunas.* Subsequently,

tion of their true stratigraphic position. The discovery, in 1889, of the
- Olenellus fauna in the shales resting conformably in the Chilhow
series, thus verifying Prof. Safford’s section, affirms the correlations s :
of 1883, except that it carries the Middle Cambrian zone above the
_Chilhowee sandstone and drops the Ocoee, if it proves to be beneath
the Chilhowee catalan back into the Basal Cambrian. :

GEORGIA.

Of the Transition, or older fossiliferous rock formation, < Georg es
White said, in 1849, that it has been Hess explored than any other pal
of the eee of Eavesin: ¢

That part of it which extends from the western” base of the primary rocks to th
Chattoogatta range of mountains, and which forms the valley of the Oostana' a

r
a
.
me
D

1On the Silurian age of the Southern Appalachians. ‘Am. Jour. Sci., 3d ser., vol. 9, 1875, pp. 279, 280. 2

3Tennessee. (Geological formations.) Macfarlane’s Am. Geol. R. R. Guide, 1879, p. 196- ze y
4The Cambrian System in the United States and Canada. Washington Phil. Soc., Bull., vol. 6, 18 23,
. ae

vey, Bull. No. 30 1886, p. 63. a

«* ~~ ° a ey “ es tw a, be >. =" nf +4 ; Pr. pee ae Se a
gs Pr, iy : tera hs ‘gu eA “s =} ‘ ~ Pel a
ick ia SS OS iia eae f re ene
i r Cbd a 5 —_ > ‘Sy 34 — J “ae b ds “- , - . * a .
esr a < ) OBORGTIA. 145,
> ok te Sas alee), J i < — A “ . - .
, : = St . .< _ =
ee : ay 4a

er, belon os probably to the older series of the New York formations, as those por-
vi oh have been examined contain Potsdam sandstones, Calciferous sandrock
es fones of the Trenton group. 7 few fossils have been found in it.!

iti 01 on ilieet fossiliferous formations are indicated by one Sams: in
thwestern corner of the State.
Pin. the case of North Carolina and Alabama, a long interval elapsed
ween the first geological survey and the renewal after the conclu-
1 of the civil war. In 1876 Mr. George Little published an account
ri geological formations in Georgia, to accompany Janes’s Hand-_
Boc ok of the State. He divides the Lower Silurian into two periods,
he hydromica schists of the copper-bearing series of the Mobile mine and Duck-
07 im , and Ocoee conglomerates and slates along the Ocoee River on the Tennessee
®, and on the Etowah River, near Cartersville, are the lowest in position of the
rocks in the State, and form a group of (2) Primordial rocks corresponding to what
= ed the (2a) Acadian epoch in Canada. The conglomerate is made up of feld-
r and a bluish quartz. The slates are hard and siliceous. This group of rocks is
erlaid in the Cohutta Mountains, and on Pine Log Mountain in Bartow County,
7 Be raidstoxe ealled the Chilhowee, from a mountain of that name in Tennessee,
orresponding to the Potsdam sandstone in New York, * * * and belongs
also to the (2) Primordial period and to the (2b) Potsdam epoch. This sandstone
ppe eet in the north of Haralson and Paulding counties, and in Yonah Mountain,
te County, and Tallulah Mountain, Habersham County, being at all these piaces
aite =< into gneiss by metamorphism.
; Th s next period, called (3) Canadian, embracing the (a) Calciferous * * * of New ©
for’ _* * * the (b) Quebec epoch in Canada, and the (c) Chazy limestone of New
orl k is represented by impure sandstones and cherty dolomitic limestones in the north-
. reste n counties; by a sandstone on the western slope of the Cohutta Mountains; and
t /metamorphic region to the eastward and southward by calcareous schists, hydro-
schists, marble, and itacolumite of the Quebec epoch, and by calcareous schists
Eo Calciferous epoch.?
s arrangement follows that of Prof. Safford in Tennessee except
tthe Knox sandstone and the Knox shales are not included.
In 1a work on “ The Commonwealth of Georgia,” prepared under the
re stion of J. T. Henderson? in 1885, there is a general description of
he zeology of the State. The Acadian or the Ocoee and Chilhowee
or rm ations and the Knox shales are all recognized. Reference to this
iption will be made in the summary of our present knowledge of
Gambrian rocks of Georgia.
lt the Tenth Census report a brief résumé of the geology i is given
ith relation to the soils formed from their decomposition. In this Mr.
we: . McCutchen states that the aggregate thickness of the groups,
stima ing the Primordial at 8,000 feet, and taking the maximum thick-
ss of each of the higher groups, amounts to about 20,000 feet. The
rir rordial and Calciferous are followed by rocks voleeced to the Quebec

tics s of the State of Georgia. Savannah, 1849, p. 22.
xeorge. Geological survey of the State of Georgia. Hand-book of the State of Georgia,
ogic map of State, by T. P. Janes, 1876, p. 37.
(of Georgia). The Commonwealth of Georgia. The country}; the people; the produce
aons. Atlanta, 1885, pp. 73-117.
Bu ul. 81- —10 oT
Gey ™

* aa - & J : :
- > te _
“a eee BP Stee sv 3 24

description of the geological formations of Bibb, Shelby, ‘Talladeg ‘dy

2 (i

7 group; first by abdut 2, 400 feet bf halen, and then by 5, 000 feet
Primordial and 2,400 feet of shales corresponding in position to to the
of Georgia, as estimated. This paper is accompanied by-a | section

crossing Dade, Walker, and Gordon Counties in northwestern Georgia. “3

‘The stratigraphic relations of the Cambrian rocks are*shown as they
oecur in Gordon County. be

organization of the geological survey under Prof. Eugene A. Smi

duction in the United States, Part 2, 1884, p. 287.

21-25.

ee en Tas ge a He sees 4 : Es
ont : eee ees » ate ~ >< % P+ > ‘ H
Bat Pe eee ose, Ale ee arg) ee doom ne SeUMeee
. =~ f in ts

ei «= _ THE CAMBRIAN. oo mare

; Fa Ets Wraith 2. cs

cherty limestones! Combining these estimates we have 8 ,000 feat 0 =

Knox shales, which gives a total of 10,400 feet for the Cambrian rocks’

A geological section of the Cambrian rocks of northwestern Georgia
has recently been published by Mr. C. Willard Hayes of the U. Sd
Geological Survey. It is referred to in the description of ihe Cambri an
rocks of Georgia.’ at ue a

ALABAMA,

The report of Prof. M. Tuomey for 1858? contains a very general
description of the formations of the State, and on the accompanying:
map the Silurian and Devonian formations are included under one
color, so that it is impossible to differentiate that portion of the Silu-
rian formation Which has subsequently been found to belong to— he
Cambrian group. Ina general north and south section, showing th eo
disposition of the strata, the Silurian and Devonian rocks are repre-
sented as unconformably subjacent to the Coal Measures and mountait :
limestone. ae

A long interval elapsed between the work of Prof. Twomey’ and the

In the report of progress of the latter, for the year 1875, a gene

and Calhoun Counties is given. In this area there is a large deve op-
ment of metamorphic rocks described by Prof. Smith in the Teport fc
1874.4 Of this series he eye ; ae:

line to the northeast corner of Chilton County, a stratum of crystalline limestor D,
almost pure carbonate of lime, may be traced by its occasional exposures. * * ‘ ;
Succeeding this limestone and apparently overlying it conformably * *
series of semi-metamorphic strata between 15,000 and 20,000 feet in thickness, st see
ing northeast and southwest and dipping at hip angles (45°) southeast. This se
beginning below, is composed of greenish gray hydro-mica slates (talcoid slates, n
reous argillites falcon slates), passing upwards into a conglomerate by enclos

with greenish siloetbig- schists. The quartzite in places i is & thin bedded silici

slate, again a thick-bedded quartzose conglomerate, and still again a lamina ¢

quartzgse or arenaceous rock, not very coherent, and enclosing small grains of 1 De
lNorthwest Georgia. (Geologic description.) Tenth Census U. §S., vol. 63 Report on Cotton I ; ,

2The overthrust faults of the southern Appalachians. Ball. Geol. Soc. America. Vol. 2, Feb1 ., 1891,
p. 143, pl. 3- | “4
8 Second biennial report on the geology of Alabama. Montgomery, 1858, pp. 168, co aa Es
4Geological survey of Alabama. Report of progress for 1874. mata ee, ae >, Pp

eee

po Se Be ee
era

+ v0.2,
=

ee eee

BAe.

ex sia of quartzites | in their several varieties makes up the main body of the

I ountains range in Alabama.

These strata are the probable equivalents in Alabama of the Ocoee con glomerates
slates ot Prof. Safford, of the Tennessee survey, by him referred to the Silurian

ists has been referred to pa -Sildzian and pre-Cambrian age. My own observations
he field while inclining me to the latter view, have not been sufficiently extended to

ble me to form an independent judgment on this point. * * * Mr. F, H.
d ley refers to the Lower Silurian all the metamorphic rocks of North Carolina as

east as Franklin.!

t

i _ This metamorphic belt is apparently the same as the altered Silurian
ocks of Prof. Bradley, as stated by Prof. Smith, and also of the altered
rc ks ale the northward extension of the Blue Ridge through Ten-

" uaidivision’ as found in Prof. Safford’s published volume.”
Jude the caption of ** Lower Silurian,” the ia igi or Cambrian

the exact equivalents of Safford’s Ocoee slates and conglomer-
S ‘2 The direct superposition of the sandstone referred to the Pots-
n, upon the Acadian slates, is not well shown in Alabama. The.
tion consists of fine-grained conglomerate, heavy-bedded sand-
ne, and sandy shale. The most characteristic markings of the rocks
this formation are the sandy rods, caused by the filling in with sand
e burrows of a marive worm, Scolithis linearis.‘
e Knox sandstone and. Knox Shales are referred to the Canadian

yeriod, thus following Prof. Safford’s arrangement in Tennessee. The

ta

yn to him. The sandstone is a calcareous sandstone associated se

( ite contains beds of blue limestone similar to those in the upper
¢ of the shale. This report contains much detailed information of
rata referred to the Cambrian in Alabama, and will be principally
Mt n the description of the Cambrian rocks of that State.

7 _ paper on the iron ores of Alabama, with special reference to
- geological relations, Prof. Smith states that the Potsdam sand-
frequently contains large amounts of iron, principally as limonite.
-Kahatchee hills, in Talladega County, the sandstone is some-

impregnated with iron in the form of specular ore or as magnetite.

> ‘Op. cit., p. 14.

x sandstone is considered to rest upon the sandstone referred to |
-otsdam, but no contact of the two formations in such a positionis -

-
s

BSR Mere Oe. Bare te UNE Rance Pare be),
im? Phung 4 ; Ps Ree ' * Ae '
sh saath ys TEA. Shoe ae BAG Te, Pe ae bas See ae
‘, ‘ - Tita sy eT : = a ox, SP ee at
os ed x t24 ne Nal
x ‘ A f aS ye EEE at oe py = ene Dy ae
ys ‘ q 2 Ar 7 *% > a A, ce a3 ‘ Pied - —_
a. sé = a's rs ain Ae S4 “I
Re 7 r fs P tas fa ay Re Hl, ae

2 Bi Lege ee aes Bf “THE: ‘CAMBRIAN, SN eS Pee. ie

~~ w

Sank beds of limonite are found. in the Knox uantiatolia ‘and. Pee c 3

-shales.!' In 1878 the same writer published an outline of the geology
of Alabama accompanied by a map of the State, based upon that of
- | Tuomey, published in 1858. Of the age of the metamorphic rocks he —
says that until further examination he leaves the question of age an
open one, except in two instances, in which he believes at least a part

of them are metamorphosed Silurian beds. | BF
The classification and general description of the formations is essen- a
tially the same as that contained in the reports of 187475. oe a

eS In a report on the physico-geographical and agricultural features ¢ 0}
Piaisiaiies Prof. Smith notes the character of soil produced by the ro a
of the different formations, from the Potsdam to the Coal measures.>
This paper was also printed in a general description of the State of
Alabama, in vol. 6, of the Tenth Census. | ,
A brief description of the Cambrian rocks of Mlabesn is given by
Prof. Kugene A. Smith, in a report on the geological structure and de-—
scription of the valley region adjacent to the Cahaba coal field.
-—- summary of it is given in the rapt te sp of the Carat rocks’
~ Alabama.
References are made to the geology of Ataburhes ina general wa v5
by Dr. T. S. Hunt, Prof. Smith, and various mining engineers, but I
have not, with the exception of fie preceding notice, met with original X
ponedintiond to the knowledge of the Cambrian rocks, since the pad)
et - lication of Prof. Smith’s detailed description.

J

>
a’ ee
The Ms
~

Wet

eq op!

PALEONTOLOGY.

1 NORTHERN APPALACHIAN DISTRICT, ~—

‘ The first discovery of fossils in rocks, now referred to the Lower
_- Oambrian, was made by Dr. Asa Fitch.’ In the summer of 1844 he
found trilobites in a black slate in Washington County, New York

— 7

-. which was referred by Dr. E. Emmons to the Taconic slate or Argillite
-. (Lof Eaton). Dr. Fitch sent the fossils to Dr. Emmons, who described
-.. from them two species of trilobites under the names of Atops trilineatus
aS and Elliptocephalus asaphoides.?’ Believing that the rocks in which the

_ trilobites occurred were unconformably beneath the Potsdam sandstone,

_ S Sy
_ 1The iron ores of Alabama, with special reference to their eeoionste relations. Am. Assoc. Pre a
vol. 27, 1878, pp. 247, 248.
2 Outline of the geology of Alabama. Berney’s Hand-Book of Alabama, 1878,p.140. —
3 (Geological features and divisions of Alabama.) Geol. Survey of Alabama. Report for 1881 2
1882, i883, pp. 178-181; 192-210.
4General description of the State of Alabama. Tenth Census U.S., vol. 6. Report on cotton Pro;

»

~~ *
ie. i*

duction in the United States, part 2, 1884, pp. 19-69. - - obke
5 Geological Survey of Alabama. Report on the Cahaba coal field, MeN: Il, 1890, pp. 148-150. (Ist ue
January, 1891.) 7%

6 A Historical, Topographical, and Agricultural Survey ofthe Sonate of Washington. Trans. . ne ‘
State Agric. Soc. for 1819, 1850, p. 865.
iy _7The Taconic System, based on observations in New York, Massachusetts, ress and I R
Island, p. 20,21 Albany, 1844. : ; ba

y »: i

. En nmons called them the oldest known fossils in ‘eiaion: In the

it he peferred tothe Taconic system.

The second description of fossils was made by Prof. James Hall in
e Paleontology of New York, vol. 1, 1847. Under the title “ Deserip-
tion of fossils of the Hudson Tevde ohiD® the following species were
¢ escribed as new: Orbicula celata (p. 290), Orbicula? crassa (p. 290),
cula ? desquamata (p. 292), Theca? triangularis (p. 313), Metoptoma ?

“%
th

ph iAe description and figures are given of Olenus asaphoides, Em-
BB, on pages 256, 257, pl. 67, figs. 2a-c. In.a later publication’ he

0 of Highgate, Vermont, but did not assign them to a geologic horizon.
In peeing a collection sent to him by Rev. Zadock Thompson, Prof.

en us thompsoni and O.vermontana. The genus Bathynotus was estab-
hed to include Olenus(Peltura) holopyga. In 1861‘ the reference of

e fossils of the Georgiaslates to the Hudson River and Quebec groups,

t » authority of Sir William E. Logan for the stratigraphic position of t:

the rocks being cited.’ Discovering that the proposed generic name,
3arrandia, was preoccupied, he substituted the name Olenellusin 1862.
This is the first introduction of the name which is now given to the
Lower Cambrian fauna.

4
; ei

zenus Discinella for what he considered to be a small brachiopod, but
ch investigation proves to be the operculum of Hyolithellus micans.’
oe 1 notes on the fossils of Washington County, Dr. Asa Fitch® de-

1, James: Hotbot on certain fossils of the red sandrock of Highgate. 3d Annual Report on th®

\ at Sie State Cab. Nat. Hist., 1860, pp. ‘118-119. “Hepart upon the geology of Vermont, ak
\pp. 367-372.

My, J, ames ; Correction for the 13th Ann. Rep. 14th Ann. Rep. State Cab. Nat. Hist., 1861, p. 110,
tl, Tames : Letter on the Primordial of America. Soc. géol. France, Bull, 2°sér vol. 19, 1862,pp.
pp eiatiaiy note to 13th po Rep. State Cab. Nat. Hist. N.Y. 15th Ann. Rep. State Cab. Nat,
N Y., 1862, p. 114. ¢

fus. Nat. Hist., 1873, p. 246.
storical, Topographical, and Agricultural Survey of the County of Washington. Trans. N. x.
@ Soe. Ae 1849, 1850,

| er group. In 1860° he Saoked the genus Barrandia, to include

7 ese trilobites was changed from the Hudson River group to the Quebec —
01 up ; and a little later a strong defense was made of the reference of

‘The last reference of Prof. Hall to the fauna is the proposal of the

n some new and hapesteotly known forms among the brachiopoda, etc. 23d Ann. Rep. N. |

to any geological horizon. Prof. Adams in 1848? mentions the Cono- we

- and imbedded in a secondary deposit ; and that the fossils in the bowl-

_ Billings, E.: Palezoic Fossils, vol. 1, 1865, p. 371.

eee Palwoph yous rectus (p. 362), aummerone (?) ‘Gitenotiin (p. 8
Helminthoidichnites tenuis (p. 866), from the slates now referred isu
— Lower Cambrian. He also mentions Paleophycus virgatus Hall, Butho- *
_ trephis (2) flecuosus Emmons (p. 862), and Gordia marina of sianonhl
as Helminthoidichnites marina (p. 868). ee

' The fauna of the “ Red sandrock” of Vermont was first discovel 3 A
~ by Prof. C. B. Adams in 1847,' who sent the specimens to Prof. Jai ames
Hall. The latter identified Conocephalus, but did not refer the fossils f

cephalus and also an Atrypa, like Atrypa Roetipher ie (equivalent to.
Camerella? antiquata Billings). = =
Mr. BE. Billings, as paleontologist to the Geological Survey of Canada,
took up the study and correlation of the older paleozoic faunas, a and
was the first to assign the fossils described by Prof. Hall toa pre-Pots a
dam horizon and to correlate the strata containing them with the
Upper Primal sandstones of Pennsylvania, and the limestones of the ;
Straits of Belle Isle. 1. Sa
In 1861 he described a number of Lower Silurian fouaita. from the —
“ Potsdam group” of Vermont and assigned the following species to. the .
horizon of Paradoxides thompsoni of Hall: Palceophycus congregatus, E ae
ineipiens, Obolella (Kutorgina) cingulata, Orthisina festinata, Camerella 1%
antiquata,Conocephalites adamsi, C. teucer, C. vuleanus, C. arenosus. “=
A little later he published a note on the “ Red sandrock ” formation
of Vermont,‘ in which he refers the formation to the base of the Lowe .
Silurian somewhere within the horizon of the Potsdam and identii
~ Conocephalites from the formation. In reprinting in 1865 the article
tciestaemt in 1861° he correlates the primordial fauna of the *‘ Red san d-
rock” of Vermont with that of Newfoundland and Labrador, and refer ‘3
them to the Potsdam group, stating that there is no paleontologicé al
evidence of precise similarity of age, but-the general affinities and sco}
of the fossils and the physical relations of the rocks prove that ‘th ere
can be no great difference. i
Under the title “On some new species of fossils from the limes one.
near Point Levi, opposite Quebec,”*® Mr. Billings described the fauna *
collected by the Geological Survey of Canada from the limestone co: ey
glomerate. He designated the rocks simply as Limestone Nos. 1, 2
and 4, not recognizing at the time that the bowlders were transports a

13d Annual Report on the geology of the State of Vermont. Burlington, 1847, pp. 31.

2On the Taconic rocks. Am. Jour. Sci., 2d ser., vol. 5, 1848, p. 109.

3 Paleozoic fossils, vol.1. Containing descriptions and figures of new or little Locaat species 0
ganic remains from the Silurian rocks. 1860-1865. Montreal, 1865, pp. 1, 2.

4 Billings, E.: Onthe age of the Red sandstone formation of Vermont. Am. Jo our. Sci., 2d ser
32, 1861, p. 232.

*On some new species of fossils from the limestone near Point Levi, opposite Quebec.
Nat., vol. 5, 1860, pp. 301-324.

ant poe oe ss a As e he Hy r ee
fe ieee LEONTO OLOGY APPALACHIAN. 151
Te 0 of Upper SGasnbeian: ‘age wills: those. of the limestone mna-

“~

oa

wh: rich resembled i in character the limestone of the bowlders, was de-
pos ited in situ, and carried the Calciferous fauna. As far as I have

een 1 able to separate the species by a study of the material from the

mericanus, A. orion, A. miinaannd, Dikelocephalus magnificus, D. plani-

the same locality.
ay Bethe species described from Point Levi in 1860 Mr. U. Billings

is ? logani, Devine and Menocephalus saltert, Devine.
+ ees? Mr. Billings returned to the study of the fossils of the older

bec , as follows : The genus Obolella and the species Obolella gemma and

neeps, H.micans. On page 240 of the same volume the genus Hyo-

of ¥ Rrment. 4

\ t. C. D. Walcott ® in 1884 from the Georgia slates of Vermont,

Sc ription of a new trilobite from the Quebee group. Canadian Nat., vol. 8, 1863, p. 95,

cit., p. 210.

joz0ic Fossils, vol. 1, 1865, pp. 195-200. :

ome new species of Potsdam fossils. Canadian Nat., vol. 6, new ser., 1872, pp. 213-226, 240.

on the discovery of fossils in the ‘‘ Winooski Marble” at Swanton, Vermont. Am. Jour. Sci.,
vol. 3, 1872, p.145. Canadian Nat., new ser., vol. 6, 1872, p. 351.

ce of some new species of Primordial fossils in the collections of the Museum, and correction
iously described species. Am. Mus. Nat. Hist. Bull., vol. 1, 1884, pp. 139-154.

Cambrian faunas of North America ; preliminary studies. U.S. Geol. Survey, Bull. No. 10,

ine, D. belli, D. oweni, D.megalops, D. poe nes Arionellus cylindricus, :

e omg Raich he aad described as Dikelocephalus belli and D. oweni from :

D. selectus, and D. pauper. He also pised in this connection Ole- —

Paleozoic rocks and described one new genus and several species found |
in k bowlders, of several beds of conglomerate at St. Simon, below Que- _

ellus i is amt for the species Hyolithes micans ; j and on page 351

he Cambrian fauna of northern Vermont was further enlarged in
L by Prof. R. P. Whitfield® describing Orthisina orientalis (p. 144), ae

‘
“a

c vw a - 3 se i + a . Nee ~ ~ a 1
—P is Ar Teg ehk a Pe Sok Se Age ee eh Soe
> a 2 ry : lon = bg ue = sod ta >» aoe o ~ an
4R9 - Post 3% ~ Bie: i Boe oS RES vad oy
NS 08 Po: THE CAMBRIAN. Veoh ae ae j

a tana. The latter was referred to the new genus Meneiatte in 1885.1 a.

Mr. 8S. W. Ford began, about 1868, a study of the rocks and fossila. s
of the hills east of Troy, New York, from which vicinity the first fossi ie
of the Olenellus fauna, found in New York, were obtained. These

¥

-_- were described by Prof. Hall, in 1847, and referred by him tothe Hud- |
gon River group. Entering ne correspondence with Mr. E. Billings, sp
and comparing the fauna he found at Troy with that from below Que. a
bee, referred by Mr. Billings to the Lower Potsdam, he concluded that :
the strata containing the fauna at Troy should be referred to an equiv- f
alent harizon. In his first paper? he mentions finding eighteen species, —
eight of which are referred to described species and ten remained to be :
described. Mr. Ford published a number of papers from 1871 to 1885,3

: in which he described the rocks, and fossils found in them, that occur
- near Troy, and also a little south of Schodack landing, in Columbia”
County, N. Y. The fossils described by him are: Protocyathus rar L
Archeocyathus rensselericum, Obolella nitida, Scenella rs
emmonsi, H. impar, Agnostus nobilis, Leperditia troyensis, Microdis .
-meeki, M. speciosus, and Solenopleura nana. One of the most interest=
ing of Mr. Ford’s studies is that on the embryonic development o m3
Olenellus asaphoides. From the data thus obtained he decided that
the Olenellus fauna followed the Paradoxides fauna i in time.‘

1 Paleozoic notes ; new genus of Cambrian trilobites Mesonacis. Am. Jour. Sci., 3d ser.,vol. 29,
pp. 328-330. =
2Ford, S. W.: Notes on the primordial rocks in the vicinity;of Troy, New York. Am. Ta our, | Sei, 3 ;
ser., vol. 2, 1871, pp. 32-34. Canadadian Nat., new ser., vol. 6, 1872, pp. 209-212. SS
3 Descriptions of some new species of primordial faséila. Am. Jour. Sci., 3d ser., vol. 3, 1872, pp. 419-
422. ,
aah On some new species of fossils from the Primordial or hice 0a group of Rensselaer County, Wi me a
York. Am. Jour. Sci., 3d ser., vol. 5, 1873, pp. 211-215. Fs a
Remarks on the distribution of the fossils in the Lower Potsdam rocks at ‘Troy, New York, with d ley
> scriptions of a few new species. Am. Jour. Sci., 3d ser., vol. 6, 1873, pp. 134-140. a4
Note on the discovery of a new locality of primordial fossils in Rensselaer County, New York ke
Am. Jour. Sci., 3d ser., vol. 9, 1875, pp. 204-206. 3 +
On additional species of fossils from the primordial of Troy and Lansingburg, Rensselaer. County,
New York. Am. Jour. Sci., 3d ser., vol. 11, 1876, pp. 369-371. ee,
Note on Microdiscus speciosus. Am. Jour. Sci., 3d ser., vol. 13, 1877, pp.141,142. “a
~» On some embryonic forms of trilobites from the paiardlal rocks at i ged New York. 6.35, Jou pur.
Sci., 3d ser., vol. 13, 1877, pp. 265-2738.
Two new species of primordial fossils. Am. Jour. Sci.,3d ser., vol. 15, 1878, pp. 124-127.
Note on Lingulella celata. Am. Jour. Sci., 3d ser., vol. 15, 1878, pp. 127-129.
- Note on the development of Olenellus asaphoides. Am. Jour. Sci., 3d ser., vol. 15, 1878, pp. 129, 130.
_ On certain forms of Brachiopoda occurring in the Swedish cpantadias: Am. gous. Sci., Kk LOOF vol. 1 ! 5.
1878, pp. 364-366. *
Note on the trilobite Atops trilineatus of Emmons. Am. Jour. Sci., 3d ser., vol. 19, 1880, Pp- 182,158
_Remarks on the genus Obolella. Am.Jour. Sci., 3d ser., vol. 21, 1881, pp. 131-134.
On additional embryonic forms of trilobites from the ig ala rocks of Troy, New York.
Jour. Sci., 3d ser., vol. 22, 1881, pp. 250-259. 2
Note on the Masotery of primordial fossils in the town of Stayrcenth Columbia County, Sa 7 k.
Am. Jour. Sci., 3d ser., vol. 28, 1884, pp. 35-37. ;
_4Embryonic forms of trilobites from the primordial rocks of Troy, New York. Am. Jour, Sein
- ger., vol. 22, 1881, pp- 250-259. War age

st

£ oe i hen et Rea ee te ame G45

Eee Set af —_ ft Be er oes or ™ bee Wt
mee he SA Sale ~ *. a
orr.] ax: or a ‘PALEONTOLOGY — “APPALACHIAN, 153 :

cs 88 $6 Prof. Ww illiam B. Dwicht Ea Cae the discovery of ‘the
at } Bhat f the Potsdam zone in limestone near voRsukrepste, New York.
e § ives a » list of eleven species as follows :! :

oF Psie pinnaformis. Ptychoparia (Conocephalites) n n. sp.
Lingulepis minima. Dikelocephalus sp.

iz Lingulepis acuminata (probably). Ptychaspis sp. ,
-Obolella (Lingalella) prima. Stromatocerium ?

v Dbolella sp. Remains of crinoid columns. ge

Pi atyceras sp.

‘The review of the Olenellus or Lower Cambrian fauna by Mr. C. D.
Jalcott in 1886? resulted in the description of the following species
ol | Vermont : Climacograptus ? emmonsi (p. 93), Orthisina transversa
». 12 1), Scenella? varians (p. 127) and Microdiscus parkeri (p. 157). This
a s followed in 18873 by an account of the discovery of a number of
species of fossils from the Upper Taconic slate of Emmons in
ngton County, New York. The new species described are as

3:

cra.

-

Ptidiralcrs granvillensis. : Leperditia (I) dermatoides,
_ Linnarssonia taconica. : Microdiscus connexas.

~ Orthis salemensis. Olenoides fos di :
_ Modiolopsis (??) prisca. - Solenopleura (?) tumida.

| Hyolithellus micans, var. rugosa. ' Ptychoparia ($) fitchi.

a ie -Aristozoa rotundata. | P. (?) el avata.

I In describing a section of the Cambrian rocks in northern Variant
22 tic ce is taken by Mr. Walcott of the occurence in the upper beds of a
r a resembling that of the Upper Cambrian or Potsdam zone.‘
lh aa paper announcing the discovery of ihe angi sapien strata of the

r¢ w. B. Dwight’ identified Hyolithes billings ? (p. 143) and described
S vw Leperditia ebenina (p. 144), Kutorgina stissingensis (p. 145), and
Nenoides stissingensis (p. 147), satcelitiog the fauna with that of the
AC lle Cambrian of the Rocky Mountain province.

Ina review of the Lower Cambrian fauna by Mr. C. D. Walcott, pre-
ared | for the Tenth Annual Report of the U.S. Saar Survey, a

1 Recent : explorations i in the Wappinger Valley limestone of Dutchess County, New York. No. 5;

ry of fossiliferous Pntedata strata at Poughkeepsie, New York. Am.Jour. Sci., 3d ser., vol.

P. 131.

nd contribution to the studies of the Cambrian faunas of North America. U.S. Geol. Survey,
$Fanna of the “ Upper Taconic ” of Emmons, in Washington County, New York. Am. Jour. Sei, |
Lser., , Vol. 34, 1887, pp. 187-199.

“S Seco ae contribution to the studies of the Cambrian faunas of North America. U.S. Geol. Survey, ~“

tu, S eatoni (p. 45), Sout Washington Ooauty, and Gunperellé 5 minor yr

fae

———

ar

.-

»
>.

ti

—

- §Surv., 1890, co 598-655.

- in that portion of the head preserved.? ©

; » Mississippi Valley.

from Dutchess County, New York; Kutorgina cingulata, var. swan to-
nensis (p. 36) from northern Vermont. ag
In 1890 the following new species were described :! Trachyum vetustu
Dawson, from Metis, Canada; Phyllograptus cambrensis, from Geotptae
Vermont; Stenotheca (2) rugosa var. acuta costa, erecta, and levis, Pla a
tyceras Bain. from St. Simon, Quebec; Olenoides ellsi, from below r
Quebec, Canada; 0. desiderata, from Highgate Springs, Vermont; Con o- ne
coryphe ‘otsoulatn. from Washington County, New York; Ptychoparia
— metisensis and orga redpathi, from below sii a

SOUTHERN APPALACHIAN DISTRICT,
NEW JERSEY, ETC.

The Cambrian fauna of New Jersey, Delaware, Pennsylvania, Mary-
Jand, and Virginia is thus far restricted to the presence of the Annelid EB
poring Scolithus linearis. It is extremely probable that trilobites. and
other fossils will be found in the Granular Quartzite series, or the base Le
quartzite and the immediately superjacent shales and limestones, i a

TENNESSEE. ;

The Gambrian fannie of Tennessee consists of Scolithus linearis tubs
found in the Chilhowee sandstone; while in the shales just above the D
sandstone occur numerous Annelid trails, a species of Hyolithes like ke
H. americanus, an Ostracod crustacean, [soxys chilhoweana, and a spe- |
cies of Olenellus closely allied to Olenellus thompsoni and 0. asaphoid es.

From the upper part of the Knox shale Prof. J. M. Safford? hag a

baiinnt tis similis, Safford. ; ;

roanensis, Safford. shah w

tennesseensis, Safford.
Lonchocephalus fecundus, Safford.

Agvostus arcanus, Safford.

Lingula prima? Conrad. a
Tee

Quite a large fauna occurs at this enn in the collections of t

Geological Survey which has not yet been studied with care. As far

as examined it appears to be of the type of the Upper eS of the

-

2Tbid., p. 626.
8 Geology of Tennessee. Nashville, 1869, p. 212.

A tr rilobite was sent to the gréat exhibition in London in 1851 said

P imordial rocks of Bohemia. The exact locality from which this spe-
: cogs was not known until collections were made in northwestern

ibe icky Mountains. The specimens occur in and upon Miliéeons
cretions imbedded in the Coosa Valley shales of Floyd County and
he southwest in Alabama.

eurticet. It occurs on and in siliceous concretions found in the

a age ROCKY MOUNTAIN PROVINCE.

allatin River district of Montana. "The Canadian extension is con-
a Peer eely.. |

UTAH AND NEVADA.

Sarin the progress of the geological survey of the fortieth parallel,
Ee: the charge of Mr. Clarence King, Prof. F. B. Meek described two
oma of trilobites from Antelope Spring, Nevada, Pardowides (?) neva-
is and pesecory phe (Conocephalites) cc referring them to the Pri-
s or dial one. -
In the following year Prof. J. D. Whitney sutiieel before the Cali-

Siedam sandstone, identifying Agraulos oweni, M.and H., or a species

ada was also sent to the American Journal of Science by Prof.
itney. In this he mentions the occurrence of certain Primordial
ies, and the persistence with which these constantly recurring tri-
tes and brachiopods are found at various localities. In Bohemia

y r occur in argillaceous shales; throughout the United States, from
v York to the Rocky Mountains, in the Eons Seen or in

scriptions of new genera and species of fossils from the Middle Cambrian. U. S. National Mu-
-, Vol. 11, 1889, p. 443.

riptions of fossils collected by the United States Geological Survey, under the charge of Clar.
g esq. Phila. Acad. Sci., Proc., vol. 22, 1870, pp. 62-64.

yme fossils from Eureka, Nevada] California Acad. Sci., Proc., vol. 4, 1871, p. 200.

on the occurrence of the “ Primordial Fauna” in Nevada. Am. Jour. Sci., 3d ser., vol, 3,

‘gas, ESS Garhes ok a ee ea Pup eRe ae
. < eee E. ec 7 > 4 , + ~ os
< “4 a ;. Pa . Sas Shox ight ae Pat, os - oa, _ bee ; > pe
< =~ ‘ee ae al : : . :
OT Sasa aa | UTAH AND. NEVADA. 155.
aa oS e a > aan i” é 5
os ie ie = pet (GEORGIA.

fAtoand somewhere in Georgia. Mr. J. W. Salter! describes the
8 as Conocephalus antiquatus, comparing it with C. striatus of the

second species was described by Mr. C. D. Walcott in 1889 as Ole-

4 Th e area of Peicneati rocks in this province includes the Cambrian
mute ‘Ops of northern and western Utah, Nevada, eastern Idaho, and >

; D ia Academy of Sciences some fossils that had been collected by Mr.
H, Clayton near Eureka, Nevada. He referred them to the age of the

~

Se y resembling it; Lingulepis prima, Obolella, Conocor yphe, Para-
les, ete. A sate? on the occurrence of the Primordial fanna in —

fossils of the Lingula-flags or “Zone Primordiale.” Quart. Jour. Geol. Soc., London, vol.

cus) wheeleri, Agnostus, and Discina. Beneath the blue gray shales is ;

limestone some 200 feet in thickness all belong to the Cambrian. _

og Merritories, Prof. F. H. Bradley states that his section along the Wa-

by. Mr. J. E. Clayton, and mentioned by Prof. Whitney when calling

_ Primordial fossils in great abundance.> From the material found oy

as eres fe tage ae
Et " oe | Go aig i ate SOMES ; e.5 Pv ee oe Be. Ne
; ‘ a +. Fy Se
156 "THE ‘CAMBRIAN. EAS Ga eae

ae the Sixth Annual Benet of the U. Ss. Guslopicak Sous of. he :

satch range of Utah is not complete. The bedded quartzites, referred ¢
to the Potsdam from the character of the overlying strata, rest. unco a a
formably upon the “Metamorphic.” No fossils were found in the
quartzite or in the superjacent gray and calcareous shales. The lime- |
stone above the shales is referred to the Niagara.’ ‘i a
During the progress of the survey west of the one ee merid 5
ian Mr. G. K. Gilbert visited the Antelope Spring locality, discovered d .

attention to the Primordial fossils found there. The fauna occurs in a —
blue gray, caleareous shale, some 200 feet in thickness. In addition to
the species described by Mr. Meek, he collected Bathyurellus (Asaphis-

a massive gray limestone, 900 feet in thickness, superjacent to a vit. |
reous sandstone.? From our present knowledge of the Cambrian oa
in Nevada, the gray limestone, blue gray shales, and an upper gray

7

The section of the Oquirrh range at Ophir City, Utah, was found by
Mr. Gilbert to have, near its base, 100 feet of light gray limestone con- |
taining Conocoryphe and Dikelocephalus. Subjacent to this a mas
sive limestone with coralline mottling extends downward some 200 feet se
to an argillaceous shale, in which Mr. J. E. Clayton found Olenus | gul-
berti.2 At the south end of the Timpahute range of eastern Nevada
Mr. Gilbert also discovered a succession of shales and sandstones, in
which he found Conocoryphe in the lower portion, and above, a band
of purple ripple-marked vitreous sandstone, with bands of siliceous - |
shale.t The descriptions of Olenus (Olenellus) gilberti and O. (0.) how-
elli of Meek are printed on pages 182 and 183 of Mr. Gilbert’s. report.

In the same volume Mr. E. E. Howell states that at Pioche, Nore
the massive quartzite forming the base of the section is subjacent te
about 400 feet of arenaceous and calcareous shales of a reddish yellow
color, containing in the more calcareous portions several types. of.

Mr. Howell, Mr. Meek described two species of trilobites, Olena
howelli and O. gilberti. | : —

On the map accompanying the Wheeler survey reports, published -
in 1874, the Cambrian rocks are included ander the same color wit he
those of the Silurian. | =

1 Report of Frank H. Bradley, geologist of the Snake River division. U.S. Geol. Sarv. of os rr. mt
6th Ann. Rep., 1873, p. 194.

2 Report on the geology of portions of Nevada, Utah, California, and Arizona, examined in n the years”
187land 1872. Report on Geog. and Geol. Exp! and Survey west of the 100th a ne in cates
Lieut. Geo, M. Wheeler, vol. 3, Geology, 1875, p. 167.

3 Op. cit., pp. 166, 167.

4Op. cit., p. 169.

5 Report on the geology of portions of Utah, Nevada, Arizona, and New Mexico exandine in 1
years of 1872 and 1873. Rept. Geog. and Geol. Expl. Sur. west of the 100th mer., in charge | of | pe a
Geo. M. Wheeler, vol. 3, , Geology, 1875, p. 258. Sa

3 : ae
— GR Md
es 5 Bi ak es.
an - > 4
= ‘ ae , wand ony BOA ° jee ee >

v * a “. 3“ ne & ™. Se an ae 7 ae af “A's i se ~
NT OS re er ee eS i
ms ’ aia ee f ‘4 w > ‘ #
-

Rey < me es w i "pss Sy eh ee
= pa ae riod yaa ~ eae: . : Fe aa Mois rk Ras rE , F wi? LY
x; =: ~~ — 7 \ nm

Ge “UTAH AND ‘NEVADA. Bs Rae

<2

A a aissance ofthe Sorthweatern. portion of the Wasatch Moun-
t a ain n sin Utah was made by Prof. F. H. Bradley in 1872. He found that oe
1e ¢ est. and eastern slopes are composed of quartzite and limestone. . :
TT “Phe former, a white and ferruginous quartzite, 1,500 feet in thick-
ess s, was, referred to the Potsdam, and a band of superjacent gray
sreous shale, 1, 000 to 1,200 feet thick, to ‘the Lower Silurian. The

ion as arranged by Prof. Bradley is as follows: }

PC UED OR IME) ROGER oh cea Wenn waco sooo anes oe --- ¢ Lower
A, oe calcareous shales, 1,000 to 1,200 feet ......-.... ) Silurian.

5, White and ferruginous quartzite, base pebbly, 1,500
7 _ feet PORE Te re art NS oS Potsdam, ie

ae | 3. Blue and gray magnesian limestones, partly a ? and

lel” Mr. Clarence King describes the strata referred to the Cambie
tem. This includes 12, 000 feet of quar taites ae bee in the

He ‘says: 4

Oa omparing the quartzites and argillites with those of the Casibrtee section in

WwW: ales, the likeness is too great to pass unnoticed, and in view of the enormous de- 3 3=——

velc lopments of these low-lying rocks, as compared with the Silurian lying above the *
Primordial horizon, I have determined to draw a line at the upper limit of the Pri-

mordial period to include the uppermost members of the Potsdam epoch and to con-

sid der the whole underlying conformable series as Cambrian down to the point of

‘the sir nonconformity with the Archean. In the extreme east of our work, inthe re-

rion of the Rocky Mountains, the Cambrian formation is of variable thickness and

ee here reaches an exposure of over 100 feet. In middle Nevada the uppermost zone ;

‘a _ the ‘Cambrian, equivalent to the calcareous and argillaceous shales of the

Wahsatch, is an immense body of dark limestones at least 3,000 feet in thickness

os rrying Primordial fossils throughout; the downward continuation of the series

being there entirely hidden by the overlying Quaternary desert.?
=
r. This general definition of the Cambrian is accompanied by a list of |

the fossils described by Messrs. Hall and Whitfield.

3 “The Cambrian section of Big Cottonwood Cajon referred to by Mr. .

King is described by Mr. S.F. Emmons with more detail. On the

‘west side of Box Elder Peak, near the little village of Call’s Fort,in

a b ody of dark blue argillaceous slates in the lower portion of the Ute —

li eee body, Mr. Emmons states that the following fossils of the .

Qu ebec group were found: Dikelocephalus wasatchensis, D. gothicus,

Ore picephalus (Loganellus) quadrans, and Lingulepis ella.t In the sec- |
) on Muddy Cafion, within 25 feet of the base of the series, occursa

ay y of calcareous shales, interstratified with narrow beds of a dark, ar

rh

ax plorations of 1872; United States Geological Survey of the Territories, under Dr. F. V. Hayden; ; = i
ike e River division. Am. Jour. Bel, 3d ser., vol. 6, 1873, p. 194. yh

. >
é 4 ci isy bP 405.

Abe
ee

Bade he Ae rooming x Sey ie SR as ote
SA earth Oe hes. Go is a ee

ae we Soe os = ne as rn ‘CAMBRIAN. - s ey ae

- fine- grained limestone, whieh contains abiticny tepaae ene 1S
_ Two species were recognized, Dikelocephalus quadriceps and Conocep-
phalites subcoronatus.’ The reference of the fossils at Call’s Fort and :
_ Muddy Cajon to the Quebec group was on the authority of the paleon- »
tologists. More recent studies of this fauna, by Mr. Walcott, in con- —
- nection with the section at Big Cottonwood Cafion prove that the faun. a
- mentioned at these localities is a portion of the Middle Cambrian fauna, —
and that the Upper Cambrian strata are absent in the section by no M

: feet beneath limestones referred to the Devonian, there were obtained —
from a shaly limestone three forms of trilobites, which Mr. Emmot ae

_ in which numerous trilobites and primordial fossils occur.’
quartzite. Among the organic remains of this range two species have Bs

of central Nevada, Mr. Arnold Hague mentions the presence of obscure | 4

— lower beds along the greater part of the ridge, occurs the Pogonip lime pv 4

of from 3,000 to 4,000 feet of strata. They dip with an angle of 24° t :
800° iceorsed: The lower beds are a fine-grained, somewhat siliceous, :
- black limestone, varying considerably in compactness and bedding, and
_ frequently passing into caicareous shales. Higher up in the Series, they
develop more of a dark blue color, banded with layers of fine arena:

d _ From the lower beds of the limestone series he collected thirteen spec: es

_ of Upper Cambrian fossils.

that at White Pine, and carries throughout the greater partof the forma: be

Clarence King, vol. 2, 1877, pp. 542,543. ~

. 2 : ‘ Oe gh RS a ghee et ra
4 Xe sa ~~ 7 — a io e jr

iy

deposition. a
In the Weber Cafion region of the Wasatch Mountains, 800 to 1 000.

thought probably indicated the horizon of the Potsdam group. ‘One! 5
was identified as Ogygia parabola and another as Crepicephalus allied to ‘
0. diadematus.? a

In the Oquirrh Mountains, at Ophir City, Utah, the section discloses |
a thickness of about 400 feet of compact reddish white Cambrian —
quartzite, above which are about 100 feet of greenish yellow clay slate,

In the Schell Creek Mountains of Nevada there are limestones. iy :
which primordial fossils have been found overlying heavy bodies os
been identified : Crepicephalus (Loganellus) anytus and Lingulepis mera. “4

At the northern end of Pogonip Ridge, of the White Pine Mountains 3

outcrops of mica slates and black arenaceous and argillaceous slates
and shales, in turn overlaid by an undetermined thickness of a compact, _
vitreous, steel-gray quartzite, closely resembling the Cambrian quartz- —
ites of other Nevada localities. Above this quartzite, and forming the

stone, which extends to the top of Pogonip Mountain, with a thickness —

ceous limestones and occasional cherty bands a few inches in thickness.>

Mr. Hague states that in Hureka mining district, northwest of. White e
Pine, the section of Prospect Mountain has the same lithologic habit as.

: vie

10p. cit., p. 410. 3Op. cit.,p. 444, | eS
2Op. cit., p. 377. 4Op. cit., p. 486. San
Hague, Arnold, and S.F. Emmons: Descriptive Geology. U.S. Geol. a of the 40th Par. 5 2

b to. the Upper Carbriat fauna.!
- The collections made by the officers of the Fortieth Parallel Survey
v peated and reported upon by Messrs. Hall and Whitfield. Of

base of Ute Peak, Wasatch range, Utah, they state that the fauna
eferred to the Quebec group on the Gewteucs of the Brachiopodus

1 n with the fauna which they refer to the Quebec group. .
In the ere review of the Paap of the bike ae parallel,
, at

lear ridges, and that the lower beds have not Rigas been brought
p to the surface. Under the term Cambrian he includes all of the rocks

Primordial, ibaa iiatas approximately the eastern nomencla-
re. In describing the rocks referred to the Cambrian he says: .

‘
é ras, the locality at the mouth of Big Cottonwood Cajion must remain as the finest
mple and the stratigraphical type. The lowest member—the Cottonwood slates,
r up about 800 feet thick, which here rest upon highly metamorphic Archean
S s—has thus far yielded no organic forms. Though searched by us with consid-
are, it presented no indications of life. The rocks are dark blue, dark purple,
olive-green, and blackish argillites, all highly siliceous, and as a group sharply
> from the light-colored quartzitic schists which conformably overlie them,
us second group, by far the greatest of the, whole Cambrian series, is a continuous
of. schists which have a prevailing quartzitic character, though varied with con-

Survey of the 40th Parallel, vol. 4, 1877, pp. 199, 200.
pes]

a. aii to fin Lower Cambrian zone, and have abhi gin com- es

a Th us far, among the reported occurrences of the rocks of this horizon in the Cor-.

ble amount of argillaceous matter. It would seem to be the product of afine-
od d arkose aera ry simply compressed into gouee schists. From 8,000 to 9,000 —

“Tames, and R. P. Whitfield : Paleontology (of the 40th Parallel). General remarks. U.S.

Feet - apie, eke pater bo ke. SIS itS Deane Lars ace pee
i Twas aS of ape so Oy ye eS) \ 5 a
* ieeii Sri ae FS Se E Gist gw a

? ~ a ars a ! “a :. 7 yee os 5 we ps et
frees’ 160 Re “THE CAMBRIAN. pam hate aces SE
tH Se he es Pipers ets

Usoapk: that in the region of wie Peaks: are some phlogopite schists and siliceous.
"zones carrying considerable muscovite. The phlogopite members recur in the Egar 4
Cafion region. The prevailing:colors of this member are gray, greenish ; gray, drab, |
and pale brown; never dark colors. Conformably overlying it are 2,500 to 3,000 feet ti é
of cream-color a salmon- color and white quartzites and quartzo- -feldsites. ‘Conia
_ sional sheets of conglomerate are seen in the quartzites not far below the summit ¢

the Cambrian.! : ; a

+

-—- The details of the Cottonwood Cafion section to this point have 1 not
been quoted, as these rocks are beneath the line provisionally drawi 1 ;
between mhe sherds and spt sumhip rocks. This will be noticed:
: province. Above the quartzite series there is a thin series of green “
'_ siliceous argillites which are usually not more than 75 or 80 feet thick, —
in which fossils of a Primordial typehave been found. A description i Ss
. given of the Cambrian as recognized in central Nevada, and a compari-
gon made between it and the Cambrian of the Mississippi Valley and
the Wasatch section. A. complete list of the fossils of the Utah an d
Nevada Cambrian is given on page 231, and on page 233 a list of those —
from the Quebec group, eight of which are from the Middle Cambrian.
zone, and will be mentioned under the description of the Cambria un
: fauna of the Rocky Mountain provinee. The geographic distribution
_. . of the Cambrian rocks and their mode of occurrence, as shown in cross- “
section, is represented on the sheets of the atlas. acooln pany ia the
‘ report. a a
ae In 1882 Mr. Arnold Hague published a preliminary ie on the
- geology of tke Eureka district,? which was followed in 1883 by the e
abstract of a report on the geology of the district.* In this latter r re-
port a detailed description is given of the Cambrian rocks of the Pro OS-
| pect Mountain section. It is accompanied by a map of the district ax nd
Ae i 7h plate of sections showing the relation of the Cambrian rocks to the
mie superjacent formations. 53
- Phe fauna of the Cambrian rocks of the Eureka district was”
- geribed and illustrated by Mr. C. D. Waleott in 1884. A short josaity p-
tion of the range of the species is given, also a tabulation of the Paleo:
- goie section of Central Nevada, showing the vertical range of genes) i
This was republished in 1886 with greater detail,’ accompanied by an
original description of the Big Cottonwood Cajfion section (pp. 38, 39),
‘anda section in the Highland range, 125 miles south of the Eureka
section (pp. 33-35), with notes upon the section at Pioche and Ophir
345 <Oity: Se haa) SEES Sie 4. Me

~*

1Op. cit., pp. 229, 230.
* Report [on work in Eureka district]. 2d annual report U. S. Geol. Survey, 1880-81. pp. 21-35, 1
-3Hague, Arnold: Abstract of report on geology of the Eureka district, eres. U.S. Geol. S
3d annual report, 1881, 1882, pp. 237-290, 1883.
4 Paleontology of the Eureka district. U.S. Geol. Survey, Neate aS vol. 8, 1884.

Bull. No, 30, 1886, pp. “30-33,

%
Fs
i
é

Be etal: LN « Me z Z “a! \Pw ‘ ‘ yaa"
+1 = : 3 : ’ } my
M4 ~ ~ '

Yo ite, RR cae OL ee \

“Dano.

n eae to Prof J. D. Hates dated Fort Hall, fdaho, July. 7, 1872,
F. H. Bradley wrote to announce the discovery of the Quebec
up. In a limestone he found many trilobites, some gasteropods and
rack hiopods s, and beneath the limestone a compact ferruginous quartz-
which from its position he considered as representing the Potsdam
mdstone.! Near Malade City he discovered a series of limestones con-
i ing Conocoryphe, Bathyurus, Dikelocephalus, Aguostus, etc. He
s in a later report that—
at] examination of these Malade rocks was made at a none where the section

. collected by Prof. Bradley were studied by Mr. F. B.
¢, who identified the genera Agnostus, mae ae ete., ee

) © group was made to cover the horizons of the Potsdam, Calcif-
,and Chazy of the New York section. Again, thronghows the
ngs of Messrs. Hayden, Bradley, and Meek there are found many
ences to the Quebec group, of strata that belong to different forma-
. This confusion arose primarily from the misinterpretation of the
ay op scans of the eaten: Cain brian and Lower Silurian faunas

ein 1877, in the Portneui and Bannock ranges. He also vidibod
» Bear River range. Several carefully measured sections are pub-
ert a summary of the rocks referred to ap chiara: that will

oy came » within the Teton district of Prof. Orestes St. John. The
al portion of the se smane is formed of ancient quartzite, alter-

gion. ° . £

he discovery of the Quebec formation in Idaho. Am. Jour. Sci., 3d ser., vol. 4, 1872, p. 133.
y, Frank H:: Report of Frank H. Bradley, geologist of the Snake River division. U.S. Geol.
the Terr., 6th Ann. Rep., 1873, p. 201.

nary paleontological Teport, * * * with remarks on the ages of the rocks, ete. U.S.

5 fon the cestigy of the @rean River district. U.S. Geol. Surv. of the Terr., 11th Ann. Rep.,
§67-572, 599, 613-616.
rl a: perokion) field work of the Teton division. U.S. Geol. Surv. of the Terr., llth

ty = ies RR ae ee eas eh SO A get tae ee RAIN, Soa Sie ce Cet iE
A “e ; ean x! Re
y, am a ‘/
ot -
¥

~ of as probably Middle Cambrian.° :

a ons are
Te Px 7 a riers ae
As x , , 25 ‘ vik’ ‘ es ee ee ee
= 3 P “ 2 it ry os ‘ fis vos be - te a =
162-3 Ped tt) CAMBRIAN. - I a

»

On the map accompanying the twelfth annual report of the Hayden
survey, issued in 1833, the geographic distribu tion of the strata 2 re-
‘ferred to the Silurian whick includes the Cambrian and the quartile :
referred to the Potsdam and a portion of the limestones referred to the a
Quebec) is delineated as it occurs in southeastern Idaho. This is based h
on the work of Messrs. Bradley, Endlich, St. John, and Sei of the a
Hayden survey. a
MONTANA. = a

During the field season of 1872 Dr. F. V. Hayden made a geolo
reconnaissance of certain portions of Montana and noted the presence <
of limestone on the Gallatin River, above Gallatin City, that contained
numerous fossils. The thickness of the entire series of strata referred
to the Lower Silurian is estimated at 1,600 feet. The massive lime-
stones referred to the Potsdam group are about 400 feet thick an d
pass gradually down into 50 feet of thinly laminated, cherty limestones ag
or calcareous mud layers, with abundant organic remains. These are
separated by a purplish sandstone that rests upon variegated sha.
clays, yellow, green, etc., then hard, dull purplish brown quart e
sandstones, which in turn are underlaid by alternating soni
and clays, the whole having a thickness of over 1,000 feet! = _

The fossils collected were studied by Mr. F. B. Meek, who identillal
the genera Lingulepis, Conocoryphe, Bathyurus, Arpt Hyolithes
and Agnostus from the beds of the east side of the Gallatin River.? -

Strata of “ Primordial age” were discovered by Messrs. Dana ant
Grinnell upon the southwestern slope of Little Belt Mountains and t the
south extremity of the Belt range of mountains; these are referred t to

with certainty, owing to the finding of Prion tial fossils.’ 5

In 1884 Dr. F. V. Hayden revisited the Gallatin River locality, i I
company with Dr. A.C. Peale.t The section near the mouth of 1 th €
Kast Gallatin River was studied in detail by Dr. ae and -two litho
logically well defined groups determined. : ag

In the report of the following year the East Gallatin group is spok cel

In his administrative report to the Director of the U.S. Geologial .
Survey for the field season of 1889, Dr. A. C. Peale tabulates the Ge al
- Jatin River Paleozoic section, sil includes under the.Cambrian t
Gallatin limestone, 835 feet in thickness, and the Gallatin sandstor ne
415 feet. Beneath the Gallatin limestones are 5,000 feet of conglome er

1 Report of F. V. Hayden, U. S. Geol. Sur. of the Terr., 6th Ann. Rep., 1873. p. 72. : : 3 Li

2Preliminary paleontological report, . . . with remarks on the ages of the rocks, ete. “ *
Geol. Sur. of the Territories, embracing portions of Montana, Idaho, Wyoming, and Utah; 6th .
Rep., 1873, pp., 431, 432. @ i,

3Geological report. Report of a geological reconnoissance from Carroll, Montana Tereitory
the Upper Missouri, to the Yellowstone Park and return, made in the summer ot 1875, by Wm. | Lu
~ low; 1876, p. 22. a
~ 4Administrative Besar Montana Division. U.S. Geol. Survey, 6th Ann, Rep. 1884-’85 . 1885, DE
51.

5Tbid., U.S. Geol. Survey, 7th Ann. Rep. for 1885-’86, 1888, p. 86.

( Raisenvery of rocks of Cambrian age in the western portion of
od Columbia is of recent date. During the summer of 1883 Dr.

bs
>

1M . Dawson and Mr. R. G. McConnell investigated the Paleozoic rocks
n e line of the Canadian Pacific Railroad and discovered at the Crow
lest Pass" a great thickness of limestone of Devonian age, beneath
hich is a great series of slaty and quartzite rocks. No fossils were
nd in the beds, but some were found in detached fragments, which
eferred to the Cambrian.” In the report published in 1886 Dr.
}. M. Dawson says that of the rocks referred to throughout his report
| Cambrian no complete general section can be offered. Along the
ne of the Columbia Valley the basal beds were not observed. The
n om ponent beds of the great Cambrian series are, in the main, quartz-
sand quartzitic shales, passing into argillites, occasionally ineluding
mes stones or more or less calcareous or dolomitic materials and con-
lo erates. :

Ne ear Waterton Lake a ‘section was measured 3,000 feet in thickness ;

ft he outcropping Cambrian beds of 11,000 feet, and it included
either the summit nor the base of the series. Other Sections were
e asured, but none were found in which the whole volume of the form-
jon could be ascertained.

Dr. Dawson compares these sections with that of the Wasatch Moun-
i ins of Utah; and more recent discoveries have shown that they are
ite similar in character. If the view of separating the pre-Olenellus
s from the Cambrian is accepted, most of the South Kootanie
as Be cscka will be referred to the Algonkian, corresponding in this
S| pect to the Algonkian (?) of the Big Cottonwood section of the
ateh Mountains, Utah. ;

2 a . Dawson farther states that Mr. H. H. Winwood announced the
scovery of Cambrian fossils in the Kicking Horse Pass in a letter
the Geological Magazine in 1885.° From among the specimens
o- at that time Mr. C. D. Walcott recognized Olenellus howelli
id Olenoides levis, trilobites characteristic of the Prospect Mountain
oup of Nevada.*® Numerous other references occur in Dr. Dawson’s
in connection with the deseription of the local details of the

\ amin nistrative Report, Montana Division. U.S. Geol. Surv., 10th Ann. Rep., 1890, p. 131.
Dawson, Geo.M.: Recent geological observations on the Canadian Northwest Territory. Science,
Bd p. - 648.

Jat. 49° and 51° 30’. Geol. Survey Ganaas, mew ser., vol. 1, 1886, p. 157B.

cit., ae ‘
Tic lage ‘of the Rocky Mountains. Geol. Mag., new ser., dec. 3, vol. 2, 1885, p. 240.

Lit y report on the physical and geological features of that portion of the Rocky Mountains
Y en Tatitades 40° and 51° 30’. Geol, Surv. Canada, new ser., vol. 1, 1886, p. 140B.

' _ , 5

eres:

a

CANADIAN EXTENSION. >

no the er at South Kootanie Pass had a min inum (estimated) thickness

__ ria oweni M. and H. on the Cascade River in débris brought down from m
the mountain, were the presence of the Cambrian in the Casc a

Be PS SS ee gh Fe DP ea ee Ae ee See es RMON EN eee
we “ > - 208s, ES en hs roe ae <> ~~ * gi ee Sate tesa ig a *
» vo” " “6 2 * ost e “ve Bs. "WA Fo ue
Pm; ; me ,

164. et CAMBRIAN. ae INES pe

upper part forms the base of the Lower Silurian (Ordovician). Beneath 1

-Paradoxides was found; and a third zone, between 3,000 and 4 ,000 fe

- Surv. Canada, Ann. Report, new ser., vol. 2, 1887, pp. 24-30 D.

¥ ‘ x m
~ } Gi - ss Po

2% 4 A 7 oghe ake J ae
_

aliens Oud of Hess refers to the Asidinig of. a specimen of Ptyohog a

Mountains.! é a | 4

An admirable map accompanies Dr. Dawson’s report, and ino ag
the region between latitude 49° and 50° 30’. The geographic distrib ee
tion of the Cambrian quartzite series and its relations to the ee .
cent Carboniferous and Devonian rocks is delineated, and their strati-
graphic position is shown in an accompanying diagrammatic sections

When exploring the Yukon district in 1887 Dr. Dawson ? discovered >
that the country north of Dease Lake had a granitic nucleus with Paleo- 0-
zoic rocks on its flanks, ranging from the Cambrian to the Carboniferous. 5
No details are given. a

The detailed exploration of the Paleozoic rocks west of the grez
Archean area, near the border of British Columbia and Alberta, wai
undertaken by Mr. R. G. McConnell, and his results are presented
in the annual report of the ipivepunt tas Survey for 1886. -The Castle
Mountain group, a great limestone formation, has a known minimum
thickness of 7,700 feet. The lower portion is of Cambrian age, and »

the Castle Mountain group the Bow River series forms a great ee
ness of dark colored argillites, associated with some sandstones, quartz 2
ites, and conglomerates. The portion exposed has an estimated thick k
ness of 10,000 feet, and in the upper part of it occur the fossils men
by Dr. Dawson, Olenellus gilberti, etc. The occurrence of fossils of
Cambrian age in the lower portion of the Castle Mountain group is
noted on page 28D of the report. 4
The fauna from the slates or shales at the teas of the Castle Moun
tain group, in the Mount Stephen section, was described by Dr.
Rominger in 1887,* and reviewed by Mr. C. D. Walcott in the Som ing g
year.
In noticing the two papers just mentioned Mr. R. G. McConnell giv
a résumé of the section at Mount Stephen. He states that no fossil is
have been detected in the lower part of the Bow River series, but spec
mens of Olenellus gilberti were found by Dr. Dawson in 1884 about. 20 0
feet below the top of the formation. The next fossiliferous zone occur
near the junction of Bow River and Castle Mountain groups, v vi

a

YL

a
a

higher up, carries the fauna described by Dr. isowinyted

10p. cit., p. 143B.
2Notes on exploration in Yukon District— Beka vol. 10, 1887, p. 165.
*Report on the Geological Structure of a portion of the Rocky Mountains, with a section. Ge ec 60)

4 Description of Primordial fossils from Mount Stephens, Hcitivnet Territory of Canada. Phila
Acad. Sci. Proc., 1888, pp. 12-19, Pl. 1.
6 Cambrian fossils from Mount Stephens, Am. Jour. Sci., 3d ser., vol, 36, 1888, pp. 161-166. 3
6 Notes on the geology of Mount Stephen, British Géiniitlad American Goslegins; vol. 31 889
23-25,

“

eee —

yeah M. aston states : that the Olenellus fauna has been
und 3,000 feet down in the Bow River series.!_ He refers the Niscon-
th, and the lower 15,000 feet of the. Selkirk series, of the Selkirk sec-
ion to the Cambrian, rae correlates them with the Bow River and lower
ortion of the Castle Mountain series of the western side of the Rocky
V fc untains. (The details of these series are given in chapter Iv, of this
ap y r.) a

-*; PALEONTOLOGY.
J

The first description of Cambrian fossils from the Rocky Mountain
novi ince is that by Mr. F. B. Meek, in 1868, who described from the
ay rial discovered by Mr. Clayton at Silver Peak, Nevada, Ethmophyl-
f these species to Archzocyathus, making A. whitneyi and A. gracile.
n 1870 he added Paradowides? nevadensis and Conocoryphe (Conocepha-
t kingi, from Antelope Spring, Nevada. From the known position
f the | genus Conocephalites the two species were referred by aie to the
ri mordial zone.*
J thd Prof. J. D. Whitney calls attention to the occurrence of the
rimordial fauna near Eureka, Nevada, at a locality discovered by
as. . Clayton. He identified a species closely related to Agraulos
ywoeni of Meek and Hayden, and fragments of the genera Conocoryphe,
= doxides, Lingulepis, and Obolella.> A notice of this discovery was
etsted in the proceedings of the California Academy of Sci-
* ces sin the same year. (Vol. 4, p. 200.) .
rom the Upper Cambrian poli of southeastern Idaho and southern
ana, Mr. F. B. Meek described in 1873 Iphidea ?? sculptilis (p. 479),
s bidens (p. 463), Conocoryphe (Conocephalites) gallatinensis (p.

saphiscus) bradleyi (p. 484), Bathyuriscus wheeleri (p. 485, foot-note).
is stated on page 465 that Bathyuwriscus (Dikelocephalus ?) truncatus
lescribed in the report. It does not, however, appear in the text.
. 5 also identified the species Acrotreta subconica Kutorga (A. atten-
— uate @ proposed if it proved to be a distinct species, p. 463), Hyolithes
garia M. & H., Camerella calcifera Billings, and Agnostus josepha,
[al - Numerous givens references are made from the fragments in the

lection, and in the lists from various localities species of the Calcif-
us zone of the Lower Silurian (Ordovician) occur, especially in the
f the collection from Malade City.°

. Geol. Soo. America, vol. 2, 1891, p. 171.

jiminary notice of a remarkable new genusof Corals, probably typical of a new family, * * *

» Silurian rocks of Nevada Territory. Am. Jour. Sci., 2d ser., vol. 45, 1868, pp. 62-64.

20n Ethmophyllum and Archwocyathus. Am. Jour. Sci., 2d ser., vol. 46, 1868, p. 144.

F. B.: Descriptions of fossils collected by the U.S. Geological Survey, under the charge of
King, esq. - Phil, Acad. Sci. Proc., vol. 22, 1870, pp. 62-64.

on the occurrence of the “ Piianecdial Fauna” in Nevada, Am. Jour. Sci., 3d ser., vol. 3, 1872,

iminary paleontological report, * * * with remarks on the ages of the rocks, etc. U.S.
arv. of the ‘Terr., embracing portions of <— Se, Wyoming, and Utah; 6th Annual

_ PALEONTOLOGY—nocKY MOUNTAINS. . < 165,

m whitney and LE. gracile. Shortly after he Sa the reference

: DF Bathgirus ? haydent (p. 482), B. serratus (p. 480), Bathyurellus _

c 5 RSI Se PS Ce PS Os oer as or eae ce i; “i
i Pa ee ree a eae age Ss ae sa hl Pee fa 5 ate Ae
F . : ‘ 4 * a og in Red Poa | - mae x nore ‘ s
Din byte aaa ia aCe Pep ee Bir ye
7 = Es oa . ; iM -¥ : = x SS
Pe paar oS, (ike THE CAMBRIAN. ARS Rae

=
4 > ‘
id

From the eotioohions: made by the geologists of ths Wheeler surt rey
west of the one hundredth meridian, Dr. C. A. White describes, in a
preliminary report, Cruzianalinnarssoni, 0. rustica, Acrotreta? subsidua,
Trematis pannulus, and Agnostus interstricta. He also identified Hyo-
lithes primordialis Hall ?; and published the manuscript description by
Mr. Meek of Olenellus gilberti and O. huwelli.. From the strata re :
_ ferred to the age of the Quebec group he describes Acrotreta pysid =

-cula (p. 9) and Dikelocephalus flagricaudus (p.12). The former species S
was subsequently identified by Mr. C. D. Walcott as Acrotreta gemma
of the Upper Cambrian, and the latter species is referred to the Middle
Cambrian fauna as Zacanthoides flagricaudus. The manuscript descriy af
tions of Olenellus gilberti and O. howelli by Mr. Meek were also printed
in 1875 under the names of Olenus (Olenellus) gilberti ines (0. ) hou
in the report of Mr. G. K. Gilbert.?

The species described by Dr. White in his preliminary report of 1874 s
were redescribed and illustrated by him in 1875. In addition to the
species mentioned in the preliminary report he describes and illustrat es
Concoryphe (Ptychoparia) kingi Meek (p. 40) and Asaphiscus wheeler
Meek (p. 43.)%

The two species described by Mr. Meek from Antelope Spring, Utal h,
in 1870, were redescribed and illustrated by him in 1877, under the
names of Conocoryphe (Ptychoparia) kingi and Paradoxides ? nevadensi
In the description of the latter species he gave reasons for believing th: at
the generic reference was incorrect, and that the species belonged to ar
undescribed genus. For this genus, if the species proved not tot be
Paradoxides, he proposed the genus Olenoides.* «

The description of the collections of the Fortieth Parallel Survey D D}
Messrs. Hall and Whitfield added a large number of new forms tot
‘Middle Cambrian fauna.° ‘

_ The new species described are:

Obolella discoidea, p. 205.

Lingulepis mera, p. 206.
? minuta, p. 206.

Kutorgina minutissima, p. 207.

Leptzxna melita, p. 208.

Crepicephalus (Loganellus) haguei, p. 210.
(Loganellus) nitidus, p. 212.

(Loganellus) granulosus, p. 214.
(Loganellus) maculosus, p. 215.

with descriptions of new species, pp. 27. Geog.and Geol. Sar. west of 100th Mer., Lieut. Wi
in charge, Washington, 1874, pp. 4-12. ;
naa on the geology of orn, of N eon, Utah, ee and Arizona examined in thas ear

182, 183. bd
* Report upon the invertebrate fossils collected in portions of Nevada, Utah, Colorado, New Me co
and Arizona by parties of the expeditions of 1871-’74. Wheeler’s Expl. and Sur. west of the 10 0
Mer., vol. 4, pt. 1, 1875.
4U.S. Geol. Expl. of the 40th Parallel, vol. 4, pt. 1, 1877, pp. 20-25,
*Tbid., vol. 4, 1877, pt. 2, pp. 205-246, :

aa

%
- bt «
= See As a=
- . U ae ‘S ~eas
7 4, ee se * 3 ay | 7, «
a q ca ¥ eee, .
: > bs ~~. ee

Sper pak ete

Sees
sid aos PP Siecerieses ons MOUNTAINS.

p! Bedpbaioe(Loedictiue) unisuleatus, P. 216.
a ia a re simulator, p- 218. :
he ~ (Loganellus) anytus, p. 219. =
ie ee ae (Bathyurus) ? angulatus, p. 220. : .
war? -Conocephalites (Pterocephalus) laticeps, :p. 221,

a Ptychaspis pustulosa, p. 223. |
Chariocephalus tumifrons, p. 224.
iat 2 Dikelocephalus bilobatus, p. 226.
—~————- multicinetus, p. 226.

oo

<i

= ~ flabellifer, p, 227,
_ Agnostus communis, p. 228,
neon, p. 229.

prolongus, p. 230.

___. tumidosus, p. 231.
P : 1m ‘Lingulepsis ella, p. 232. |
eo. estes subcoronatus, p. 237,
_ Crepicephalus ? (Loganellus) quadrans, P- 238,
ae Seon quadriceps, p. 240.
3 ea - wasatchensis, p. 241.

ss Fgothicus, p. 242. ee,
7 _ Ogygia producta, p. 244.
area p. 245.

OSD
vs
.

cies mentioned.

in 18° 874, to the genus Acrothele of Angelin,!

28C iption of a number of new species from the Cambrian.

ne ae the following: ?

- Acrothele? dichotoma, p. 14.

- Scenella? conula, p. 15.

- Kutorgina whitfieldi, p. 18.

: -_- prospectensis, p. 19.
Orthis eurekensis, p. 22.

a

ar

Stenotheca elongata, p. 23.

_ Agnostus richmondensis, p. 24.
seclusus, p. 25. -

-Olenellus iddingsi, p. 28.

_ Dikelocephalus nasutus, p. 40.

- riehmondensis, p. 41.

Fangustifrons, p. *

iole, p. 43.

———- marica, p. 44,

_ %expansus, p. 45.

: * _Payehoparia (?) prospectensis, p. sash

aa _ (2) linnarssoni, p. 47. tvs

eacrpin ale. U.S. Nat. Mus. Proc., vol. 3, 1880, p. 47. _
tology of the Eureka district. U. S-Geol. ap. Monograph, vol. 8, 1884, pp. 11-64.

oe ae
pre ion a b

De ere woth “ae
em eres) Cee oS pe:

Ta ES See *

Cet,

=

f these species those from Lingulepsis ella to Ogygia parabola, in- —
usive, are referred to the Quebec group, and the others to the Pots-
The descriptions are accompanied by fine illustrations of all the

a n 1880 Dr. ©. A. White referred his Acrotreta ? ‘aug described _

: The study of a collection made vy the U. 8. Geological Survey Eom t
h e Eureka district, Nevada, gave Mr. ©. D. Walcott material for the

They

5 nbs ME age ey RPS eee te ante ar Ngee tes

‘ met +X

‘
*

Sena a riisetlisetbara, “Es & W., p. 38.

ein Ptychaspis minuta, Whitfield (?) p. 60.- , sy

: Tbe. Rese rae “THE CAMBRIAN. SC eae 8
‘aaa TOS pri gee a Pe pee . ee
" Ptychoparia (2) iGalohetduets} (2) brevicer, P 49, r a ae

Rae communis, H. & W., p. 27. |

(?) pernasutus, p. 49, - ~ ; = eee
(Euloma ?) dissimilis p. aes ace als 2 A Sean
occidentalis, p 51. cay a Oe ee eae ‘ef >a
similis, p. 52. :

paso similis, var. robustus, p. 53. eae mi =)

(Euloma ?) affinis, p. 54,
leviceps, p. 54.
(Pterocephalus) occidens, p. 58. ae
Anomoceare ? parvum, p. 59. pam es .
Agraulos? globosus, p. 61. a .
Te Arethusina americana, p. 62. - <
Ogygia? spinosa, p. 63. : .
(?) problematica, p. 63. ~

The following genera and species are mentioned and illustrate a: :

Protospongia fenestrata, p. 11.
Lingulepis mera, p. 12. ;
? minuta, p, 13. - tare
Lingula? manticula, p. 13.
Obolella discoidea, H. & W., p. 14.
Acrotreta gemma, Billings, p. 17. . :
Under this species are also included Acrotreta subconica and A. atoud a,
Meek, 1873, and Acrotreta pyxidicula, White, 1874. 8 cs. ¥
Bute Kutorgina sonal tlie. Meek, p. 20. ; ee
. The synonymy of this species includes Iphidea (??) soulptilie Ieee
Kutorgina minutissima, H. & W., 1877. ee
Leptena melita, H. & W., p. 22. <a eee
Hyolithes primordialis, Hall, p. 23. . . ;
Agnostus bidens, Meek, p. 26.

‘eg

PP
mt
4 d
heel
<a
oa

_ neon, H. & W., p. 27. . * ee
. prolongus, H. & W., p. 28. - oats . -
| Olenellus gilberti, Meek, p. 29. a . ~ = an
howelli, Meek, p. 30. ; a
Dikelocephalus bilobatus, H. & W., p. 40. ; nd of
osceola, Hall, p. 40. 3 4s

? quadriceps, H. & W., p. 45. - Pe mire
Ptychoparia oweni, M. & H., p. 55. [aa
Under this species are placed as synonyms Ciaaanieds ( Ptychope 40 )
‘ gallatinensis, Meek, 1873, Crepicephalus eisai: centralis, Whi
; field, 1877. = ;
t anytus, H. & W., p.56. .
granulosus, P. aad and P. neeitan H. & W., p. 57. 7

Under the latter species Crepicephalus (Loganellus) simulator, He
W., 1877, is placed as a synonym.

(Pterocephalus) ating ee: H. & W., p. 59.

, Chariocephalus (?) tumifrons, H. & W., p. 61. ~e

‘Notes on the genus Acrotreta of Kutorga are given on 1 page 16; d
observations on Olenellus howelli on pages 32-39. a

~

] ae PALEONTOLOG"—NOOKY MOUNTAINS. - 169 _

aD Be flowing new phat were described from Utah at N Svaiine :

- Eoeystites #? longidactylus, p. 94.
. Orthis ? highlandensis, p. 119.
‘ a Ke fiyolithes billingsi, p. 134.
Leperditia ? argenta, p. 146. mtg
-Olenoides typicalis, p. 183. . .
_ levis, p. 187.
S Pischeparts housensis, p. 201.
piochensis, p. 201.
- Crepicephalus liliana, p. 207.
.- augusta, p. 208.
_ Orytcocephalus, new genus, p. 210.
~ Orytcocephalus primus, p. 210.
_ Bathyuriscus howelli, ‘p. 216.

The g genus Ethmophy lium, described by Mr. Meek in 1868, and the
p ecies placed under it referred in the same year to Archzocyathus, is
of ned as the genus Ethmophyllum, with Picea whitneyt as

Ps

ier tspecias. Descriptions and illustrations of the following
ies also appear in this work:

~ Protospongia fenestrata, Salter, p. 90.
Lingulella ella, H. & W. p.97. ~
_ Acrotreta gemma, Billings, p. 98.
- Kutorgina pannula, White, p. 105. gees ie
_* prospectensis, Walcott, p. 106.
_ Acrothele subsidua, White, p. 108.
Scenella ? conula, Walcott, p. 127.
_ Stenotheca ? elongata, Walcott, p. 129.
Bh Abeta interstrictus, White, p. 149.
nS. Olenellus iddingsi, Walcott,p. 170.
>> ~ ~~ gilberti, Meek, p.170. |.
<r Olenoides nevadensis, Meek, p. 181.
oe _ spinosus, Walcott, p. 184.
__-fflagricaudus, White, p. 185. ‘
"+ quadriceps, H. & W., p. 187.
~~ -wasatchensis, H. & W. sp-189.
_- Ptychoparia kingi, Meek (sp.), p. 193.
“* __ quadrans, H. & W., p. 199.
_-——s«sF prospectensis, Walcott, p. 202.
subcoronata, H. & W., p. 205.
a. 5: Anomocare ? parvum, Walcott, p. 209.
— productus, H. & W., p. 217.
. Epeerhipons wheeleri, Meek, p. 220.

i paper. on the stratigraphic position of the aS fauna Mr.
D. Walcott reviewed the stratigraphic position of the fauna de-
= in Bulletin 30 of the U. S. Geological Survey, and referred the

r we re gt as SiR 8 & Gyot ar ae ot = Ne RTA ER ep ee ieee ers
“170 ae THE CAMBRIAN, SE Oia a

‘Hilosing ‘species, formerly assigned to ihe Lower Gambrisn fauna, om
the Middle Cambrian zone, considering the Olenellus zone to include
only the Lower Cambrian fauna.' The species are: aS See a

“a Protospongia fenestrata, Salter. pre te i i-
Eocystites?? longidactylus, Walcott. é a Ss
Leperditia argenta, Waicott. , >
~ Agnostus interstrictus, White. -
Olenoides nevadensis, Meek (sp.).
; . quadriceps, Hall & Whitfield (sp.).
ae. wasatchensis, H. & W. (sp). |
spinosus, Walcott. -
typicalis, Walcott.
Ptychoparia housensis, Walcott.
kingi, Meek (sp.). |
piochensis, Walcott. .
? prospectensis, Walcott. .
quadrans, H. & W. (sp.).
subcoronata, H. & W. (sp.).
Bathyuriscus howelli, Walcott. | > Ug
productus, H. & W. (sp.). e
Asaphiscus wheeleri, Meek. . .
Ptychaspis piochensis occurs 100 feet above the Olenellus zone proper,
-. in the Highland range section, but as it also occurs 1,137 feet high her }
. up in the same section, it is now referred to the Middle Cambrian faun na
~ and not. to the Olenellus fauna.’
The presence of Cambrian fossils at Kicking Horse Pass of the Rocky y y
Mountain division of the Canadian Pacific Railway was announced by
Mr. H. H. Winwood in 1385.* Indirect reference was also made to this

+

by Dr. G. M. Dawson in 1884.4 The specimens obtained at that ti ne

- | were examined by Mr. C. D. Walcott, who recognized Olenellus howel
and Olenoides levis, trilobites characteristi¢ of the Prospect Mountain
group of Nevada.°

During the survey by Mr. R. G.. McConnell of the section along tl

line of the Canadian Pacific Railway there was discovered at Mount. sta

_ phen a zone of fossiliferous slate 2,000 feet above the base of the Cas Ke

Mountain limestqne. From the collections obtained Dr. C. itomin ¥@]

described the new genus Embolimus and five new species of 7

bites, Viz: Ogygia klotzi, O. serrata, Embolimus spinosa, E. rotundata

and Oonocephalites cordillere. He also identified M:nocephalus saltei i2,

Billings, Bathyurus ?, Agnostus (“compare A. interger Barr”), and t he

= genera Orthis, Obolella, Kutorgina, Leptena ?, Metoptoma, and Hyo
lithes.® 3 ‘se

r

1 Stratigraphic succession of the Olenellus fauna in North America and Europe. Am. Jour. 8 Sci.

Pars; 3d ser., vol. 37, pp. 374-392; vol. 38, 1889, pp. 29-42. =
2 Op. cit., p. 387. a
_* Geological age of the Rocky $s lag bagjees Geol. Magazine, new ser. dec, 3, vol. 2, 1885, ate * ai
5 Preliminary report on the physical and geological features of that saebtba: of the roksan
between !atitudes 49° and 51° 30’. Geol. Surv. Canada, new ser., vol. 1, 1880, p. 140B. e-
® Description of Primordial fossils from Mount Stephen, Northwest Boutsary of Canada. _ Ph ils

phia Acad. Sci., Proc., 1887, pp. 12-19. t

:
t ' 4
, ae
: sae “$3 &
: ce ae

Ae, oo ee Ti 6 OS” Se eee ey aal - i, meer Fe
oes Ghana Porn ute! eg a Re Ren ee eS
ett.
ot EE ap es

= ? a ‘ - 7 4% “ “ -

“

eee "WISCONSIN. fe Vote se Ly be

roe ore
pees : in

we 1 eview of Dr. Rominiger’s work on the Mount Stephen fossils by Mr.
| ©.D. ).Waleott resulted in his determining that Hmbolimus spinosa, Rom.=
Zac anthoides spinosus, Walcott; Embolimus rotundata, Rom.=Bathyuris-
CUS howelli, Walcott; Ogygia errati= Olenoides nevadensis, Meek ; and
a at Conocephalites cordillere, Rom.=Ptychoparia cordillere, Bain:

aly

OP eh

~ Cambrian fauna. The genus Zacanthoides is proposed to include Ole-
Rinides typicalis, O. spinosus, O. levis, and O. flagricaudus, described in 1886.

pe mositie interstrictus, Acrotreta gemma, Kutorgina prospectensis, and
_ Hyolithellus micans.. Subsequently from the collection studied by Dr,
_ Rominger there were described by Mr. Walcott, Lingulella macconelli
~ Orania ? columbiana, Acrotreta gemma var. depressa, Orthisina alberta,
Bs Platyceras romingeri, Karlia stephenensis, Bathyuriscus (Kootenia)

ated of Rominger. Linnarssonia sagittalis was also identified.? ~

In 1890 Mr. C. D. Walcott * described three new species from the
Highland range section of Central Nevada, referring them to the Upper
Cambrian. These species are Hyolithes attenuatus, H. curvatus, and-H.
a) oorrugatus.

INTERIOR CONTINENTAL PROVINCE.

_ This province includes the Upper Mississippi area, the eastern border
or Adirondack subprovince, the western border or Rocky Mountain
subprovince, and the Llano County area of central Texas and the
G rand Cafion of Arizona as a minor southwestern subprovince.

. Bus att

ae

io UPPER MISSISSIPPI AREA.
ot as : os

> Wi isconsin, Minnesota, and Iowa is assembled for each State. The
Ss Ozark area of southeastern Missouri is considered separately, and the
wake Superior sandstones and the controversy in relation to them is
“not iced under a distinct heading, after the description of the recognized
U pper Cambrian rocks of Wisconsin, Iowa, and Minnesota, and their
extension into Canada. This division also includes the references to
_ the e Cambrian rocks of Michigan.

ea i :
4 eA. | WISCONSIN.

2 1843, in notes on the geology of the Western States, Dr. D. D.
yen called attention to the presence of a sandstone on the Mississippi

AGambrian fossils from Mount Stephens. Am. Jour. Sci., 3d ser., vol. 36, 1888, p. 165.
“ sDeototon of new genera and species of fossils from the Middle ee. U.S. National
I seum, Proc., vol. 11, 1889, pp. 441-446. '

"Desc of new Faia) of bh Cambrian fossils. U.S. Nat. Mus. Proc., vol. 13, 1890, pp. 267-279.

“a *

‘> ad .

. ise ,

a Be ee 3

8 gee i ne a . >
“" 4 @- .. =

7

hee

“@p. ), and’ Ogygia ?? klotei, Rom., are new to the previously known

| There were also identified from the material studied by Dr. Rominger |

- dawsoni, and the genus Ogygopsis was proposed to include the Ogygia :

_ For convenience of reference the review of the literature pertaining 2

VE River, at. Prairie du Chien, visible beneath the Lower Magnesian lime- —

3 stone of the Wisconsin Bisak! Five. years later, i in the report of a :
geological reconnaissance of the Chippewa land district of Wisconsin, *

metamorphic roeks, in the eastern part of the Chippewa land district,
as a coarse sandstone overlaid by a still coarser quartzose sandstone.?

beneath the fossiliferous layers at Mountain Island it is stated that i in”

_ ciety of France through a letter to M. de Verneuil.®

the rock easily crumbles upon exposure; color white or red. The white variety
. of the identity of this rock with the Potsdam sandstone of the New York reports. — It 4

cae anesville, is a limestone with grains of the same sand intermixed, giving it the —

rise from the surface of the sandstone. It sista exactly with the description given

it occurs near Wolf River, etc., stating it to be a sandstone easily
c crushed between the fingers, which has been so extensively denuded —
that it is only here and there that a trace of its former existence ing

_ Secretary of the Treasury communicating a report of a geological reconnaissance of the’ Chippewa _ :

SE tee eat ey Ve one cee ee a ATS eM re ae a ee a kg Ne | here ae Te Lae
be “ , - ' : by & ~ ; mr) 2 7 wR
ae jar ree t TGs My eT PEON Py mas ale ee oka . oa 9 ie : Ny — ‘i

- oe ap , oe - ax ek ete me Se Ae i 2,

12 pened cea ie! CAMBRIAN. Peat The ct + a

- + -

he describes with considerable detail Formation 1, or the lower a aa
stone of the Upper Mississippi. The formation, as a whole, is subdi- —
vided into five parts. The lowest part rests upon crystalline and —

At the Falls of the St. Croix the schistose, silico-caleareous layers: of |
the second division are highly fossiliferous. In the third division the | |
prevailing genera are Lingula and Orbicula? and it is designated as —
the “Lingula sandstone.” In speaking of the beds of sandstone —

all probability this is the western equivalent of the Lingula beds of the
New York Potsdam sandstone.* 7

A notice of the discovery of the fauna in the lower Poe Wie of Wis.
consin was communicated by Dr. Owen in 1848 to the Gredlogient So-

In a letter descriptive of the geology of southeastern Wisconsin ade
dressed to Mr. J. W. Foster, Mr. I. A. Lapham states that— a

The Inferior, or Potsdam sandstone, is found at Janesville and above, occupying the —
bed of the river. The grains are rounded, smooth, and without apparent cement;

might be used for the manufacture of glass. The discovery, in 1849, of that singular —
and characteristic fossil described by Mr. Hall as Scolithus linearis (New York Pal. —
vol. 1, p. 2) in this rock, in Sauk County, may be considered as settling the question —

occupies much of the counties Marquette and Columbia, enters Dane County, and is is
seen in the banks of Rock River from Lake Koshkonong to Janesville. ce.
* * * II. Caleiferous rock of Eaton.—Resting immediately upon the sandstone, —

form and appearance of an oolite limestone; the amount of sand diminishing as you

of a portion of the calciferous sandstone of New York, and contains the same facoid oe
(Paleophycus tubularis), as wellas other characteristic fossils. Its character and rel-
ative position also clearly show that it is the same rock that, farther west and north,
is called the Lower Magnesian limestone, by Drs. Owen and Locke.s ah

In the same report, Mr. Charles Whittlesey describes the sandstone : ae J

10n the geology of the Western States. Am. Jour. Sci,, vol. 45, 1843, p. 164. a
_20Owen, David Dale: Report of a geological reconnaissance of the Chippewa land district of Wis-
consin, and incidentally of a portion of * * * Iowa and of the Minnesota territory. Letter of the. ,

land district of Wisconsin, etc., by D.D. Owen, Thirtieth Congress, first session, Senate Ex. Doo. § 10.
57, 1848, p. 13. The

3Qp. cit.,.p. 14.

‘ #Op..cit,, p- 16. _ ae

5 Letter on geology of Wisconsin Territory. Bull. Soc. géol. France, 2° sér., val. 5, 1848, pp. 294-296, a
s iaphes, LA.: “On the geology of the nanchbasteen portion of the State of Wisconsin, being t th ‘a

trict, 24 Foster and Whitney, part 2, 1851, p. 169.

giving | an account of his iesathieatt aie in epnneetion with the
geological survey under the direction of Messrs. Foster and brie uaicd.
. J. Hall states:

os Eire iis satiated myself that the sandstones of the Upper Mississippi are of the

same age as the Potsdam sandstones, and that the Lower Magnesian limestone of the
“Western geologists is identical with the calciferous sandstone of New York, the next
x =

ne mber of the series above the Potsdam sandstone. The thin bed of idnuissinaie sue-

aA be regarded. as a repetition of the arenaceous deposits below, which likewise alter-
, coh with the calciferous sandstone near its base. 3

4 - He thus corroborates the view of Dr. D. D. Owen that the lower sand-
“stone of Wisconsin is the equivalent of the New York Potsdam.

- In 1851 M. E. Desor called attention to the presence at St. Croix of
a fossiliferous sandstone 800 feet beneath that described by Professor
all, in which he found fossils.‘

In a paper on the paleontology of the lowest sandstone of the north-
Wi est Dr. D. D. Owen states that he observed multitudes of Lingulas
¢ and Orbiculas disseminated in strata abutting against the southwest:

ft
+

& ‘This was in 1847. During the remainder of this season and in that of
48 he found finer-grained and more laminated soft sandstones, with

- which characterize the lowest sandstones of Russia. This was in a
ction on the Mississippi, between the Falls of St. Anthony and the
m a of the Wisconsin River. From the results of these observations
he finally developed beneath the Lower Magnesian limestone at least
- ix different trilobite beds, separated by from 10 to 150 feet of intervening
‘ in the final spe on the geology of the Upper Mississippi Valley, the
8: same writer describes the lower sandstone as composed of light-colored
quartzose sandstone that forms the greater part of the formation, with
i ntercalations of magnesian limestone, especially toward its upper part,
w vhere it graduates into Formation No. 2, and at certain localities argil-
ba AceOUs, and other beds of a mixed ‘iaradter form a considerable por-
tion of its. lower mass.6 In a table of the elementary stratification of
the lowest Protozoic sandstones he places the Lake Superior -ferrugi-

3 1) on the geology of the Lake Superior land district, by Foster and Whitney, part 2, 1851, p. 174.
Pa Whittlesey, Charles: The dip, bearing, and thickness of the Silurian groups. Rept. on the geology
of the Lake Superior land district, by Touker and Whitney, part 2, 1851, p. 183.

f i dite.) Am. Acad. Proc., vol. 2, 1851, p. 254.
om oo sandstone on the river St. Croix.] Boston Soc. Nat. Hist. Proc., vol. 3, 1851, p. 202.

> ing this rock can not be identified as the Potsdam sandstone by itself, but must —

side of the trap range that crosses the St. Croix River at the falls. :

| subordinated silico-ecalcareous layers, charged with Obolus, like those—

x Romarke upon the section from the falls of Wolf River, through Navarino to Lake Michigan. ©

% y . aes Ch et Ris x ats is Bt Ne Nye Gite nae ave ames ; $. ee oe iS
ee ae ee 5 Beier ioe ~ ons ey Ch oa ae . es
- J . ~ Se s Ona rr * ; x - Hare Te | Sie Ra Paes tea
Pie ares Res ol pn Oe ee a ee
ek: THE CAMBRIAN, Pennie on
' 2 ae | aie ses ys a. .

nous and argillaceous saniistones, shales, and conglomerates at the base, .

| _ assigning it a thickness of 5,000 feet. Above this occur coarse grits and 4
~ sandstones of the Onippews: Black and Wisconsin Rivers.! The placing
of the lower sandstone of Lake Superior in this position is theoretical. —
Above the coarse sandstone the formation is divided into six trilobite —
beds, as follows: ? :

Table of the elementary stratification of the lowest Protozoic sandstones.—
Formation 1.

Feet.

degrees of induration, with intercalations of - lias
beds of magnesian limestone, with glisten- — .
: “1 as ing erystalline facets, and calcareo-siliceous
Sixth Trilobite bed. -- ‘ oolite, produced by rounded grains of quartz,

Quartzose, light-colored sandstones of various

Bees i See encased in calcareous cement, containing ~
Euomphalas and imperfect Trilobites. Lo- a
cally with a band of green earth .......... 50 to 85 —

Mammillary and botryoidal layer of white

sandstone; sometimes banded with yel- =

| rtd LO Wisco och tec pene eee 5 to 6 inches. ‘s
> : Thick beds of soft, yellowish and brown sand- 3 :
“ ( stone, sometimes with botryoidal, hard, pro- . aa
RE Seared Ws tia ole ae een jecting concretions passing downward into «
fine-grained soft sandstones approaching an
[ SELDOM s 5 ook: 5 ng eels Ces teat he coawin ae Bel 40 to 50 —
( Ash-colored and Apel aah ore ew
a “Tons and magnesio-calcareous beds, containing.
Fifth Trilobite bed. - Dikelocephalus minnesotensis. * 2 a
Stillwater Trilobite bed.-..........-..-...-.. 8to 10 ©
Green,red,and yellowishsandstoneswiththin, = = ~—
schistose, dolomitic intercalations ...-.... 40

Upper, brown dolomitic layers containing _ a
Orthis, Lingulas, and columns of Crinoidea

as at La Grange Mountain................ ‘ - oe
Alternations of yellow, laminated sandstones, a
. Fourth Trilobite bed. - with green particles disseminated.......- =e 5 3
Marine Mill Trilobite grit..........:-...... |, a
| Fucoidal layers, and thin-bedded pisen and
yellow sandstones, at their base often a ;
band of about 6 inches of green earth used

by the Indians as a pigment ........-.-... —380to 40 —
Green and red sandstones, charged with sili- Se
| d.<- Cate of {rons s. ab ecus) soap apeeens cacnn 3 —
, . Loose, green sand, and soft green sand- —
: * OOOO. 6 sian Se BEES Sacicn Meas tebe eer 15.4
{ Micaceous sandstone, containing Dikelo- il

cephalus meniskaensis, D. Searhaphen. ete me 3
Alternations of green and ferruginous sand- == ©
| Third Trilobite bed. . SECTOR es ee Te ee IN ee 20.
! Micaceous sandstones containing D. menis- a
KAONHS, CHO. Fo och Cup ats ne o's boas KRp eae - 2m
| Thin layers of green sand, alternating with Fs

green earth, imp regnated with silicate of Se
SSOM? os. doned bos ates ch dod to cog cee 30to 40
Lower, brown siliceo-calcareous and dolo-

mitic bands of Mountain Island, and else-
Where. soca te ent) oe eae ae
Soft, thin- bedded sandstones, with scales of — a
mica disseminated .. 2.2.5 ...2 see ceen Joe see 10to 15
are ep ee eo itawehpewrds Coarse lingula grit, green, yellow, sometimes 2.
PT ace'* almost white......-..--.--- i imme Sc 100 to 130

1 Op. cit., p. 53. ; : ? Op. cit.,-pp. 52, 53.

»! ont , . Ver a .
e ~~" > 2 ™ a bal

so. 17 eeu wy a> t $4" Salt
A te Se Bale -—* , aN 4 , .

Table of the elementary stratification of the Lowest Protozoie sandstones,
Sas _ ete.—Continued.

grit (7). White and yellow sandstone, and

Obolus layers of Black River ...-..--..... . 6
=’ Ferruginous Trilobite grits. Schistose sand-

; stone, containing fork-tailed Trilobite beds

, Er ‘First Trilobite bed...

Sara = Fine grit. Place of the Menomonie Trilobite
| Second Trilobite bed..
>, : ;

eno Guotos Inverts. soc. dasa. Sic ca ses lto 8

; Magnesio-calcareous rock, with Obolus and
fork-tailed Trilobite .......--.-.-.-+----+. ‘3

— Highly fossiliferous schistose, siliceo-calcare-

ous layers, interlaminated with argillaceous,

marly beds, charged with sulphate of iron;

; the former full of Lingulas and Orbiculas
Riese tid es CLOLE) = 5 nda cwniewe penn tate 50

(Sandstone, with oblique lines of deposition,

alternating with pebbly sandstones and

pr | coarse grits of the Chippewa and Black and
G... 2002 eccwes secces see--.% Wisconsin Rivers near the falls ........... 50 to 100

3 s: ‘= [ate of the Lake Superior ferruginous and

~

argillaceous sandstones, shales, and con-
glomerates .............% Scien ete eiens cateeas 5, 000

The geographic distribution of the formation is shown on the map
U ecompanyin g the report.

& The local details of the sections in Wisconsin are reported upon by
m: rof. B. F. Shumard. Much of the information here given was used
by Dr. Owen in giving the summary of the divisions referred to Forma-
tion No. 1, or the lower sandstone.1

. The Sihidatanes of the south shore of Lake Superior are described by
Mr. J. C. Norwood, and a section given of them as seen at the mouth of
Or an berry River. He also describes the sandstones of the St. Croix
R River.? :

In his annual report of the geological survey of the State of Wiscon-
pit in Prof. J. G. Percival describes the lower sandstone with consider-
‘able detail, but without special addition to the information given by
‘Dr . Owen. He separates, however, the quartz rock of the Baraboo
an 1d of Portland from the Lower sandstone.

_ The volume of the geological survey of Wisconsin, by Prof. James
fall, contains a general account of the Potsdam sandstone. The open-

in ing paragraph describes it as follows:

=<

The lowest rock of the series is the Potsdam sandstone, which is known in the north-
we b as the Lower sandstone, in contradistinction to the Upper or St. Peter’s sand-
‘one, ‘which lies above the Lower Magnesian limestone. This is equivalent to the
P \tsdam sandstone in New York, and holds in all respects the same geological position:
it is the lowest fossiliferous rock observed in the geological surveys of New York,
where it received its name.

ie rock has been traced, with slight interruptions, westward from Lake Cham-

Goal Report of local, detailed observations in the valleys of the Minnesota, Mississippi, and Wiscon-
ae | Rivers. Report of a geological survey of Wisconsin, Iowa, and Minnesota; and incidentally of
- _portion of Nebraska Territory. Philadelphia, 1852, pp. 475-531.

24Geol. Report of a survey of portions of Wisconsin, and Minnesota. Rep. Geol. Surv. of Wisconsin,
vi panna ‘and incidentally of a portion of Nebraska Territory. Philadelphia, 1852, pp.

ence A} "WISCONSIN. Re ours RED

= eee e race ting, Se nh ite A ered ty al Pe ae Pe ae eS ERO a Ng ons A a
* «ye n ”“ >

_ the West, it should not be forgotten that there is a long interval on the isiges.

Aa. > 5" =. Se LSS toy 2) eee ee Sy toh See ee oes a ,
. 7 PES ast tee - = Bp Bip | & ue aus
_— ined SPS rea SS fa 4 Vise. SS ad it A> = a
< Nata - 2 ta rene? b hein en > ass = ee. ies, Wad
~ ~ wie ~ . a Fa ee ve

176 Eee ee. THE CAMBRIAN, co ee
plain through Ganaas to ‘the outlet of Lake Superior ee along the south ana
that lake.! a
This is followed by a general account of the formation: and of the or-
ganic remains found in it.? a
In the same volume Prof. J. D. Whitney seat a brief résumé of the e.
- Potsdam or lower sandstone.? _ , < 3
-In a paper entitled “‘ Preliminary notice of the fauna of the Potsda
sandstone,” Prof. James Hall states that in 1850 he had the opporsunilal
of tracing the formations from Drummond’s Island and St. Mary’s River 1
to the head of Green Bay and thence across the country to the Missis-
sippi River. He comes to this conclusion: ; od

~ oa »

The position of the sandstone on the St. Mary’s adinitted of no doubt, and it s rele e
tive position to the lower limestone had before that time been well determined, and
the same was likewise ascertained by the several exploring parties oe different
‘lines between Lake Superior and Green Bay. _. 4
Throughout Wisconsin there is no difficulty in recognizing. the following sequence: P

Trenton limestone; y
Black River or Buff limestone;
Birdseye limestone;

St. Peter’s sandstone; td ae
Lower Magnesian inte or calciferous sandahones oe.
Potsdam sandstone. sa ,

The St. Peter’s sandstone holds the place of the Chazy limestone of ‘the. ma re re
eastern localities, and, with this exception, we have the same sequence that we fin a
in New York, many of the fossils being common to the limestone of: New York 2a
- Wisconsin. = Be
Dr. Owen, in his published report, has adopted this view of the sequence, kel the 7
explorations of subsequent years have confirmed the opinions then entertained ; an . ,
I believe at this time every geologist will admit the identity of the Potsdam sand-
stone of New York and the Lower sandstone of the Upper Mississippi Valley. - ~

In speaking of this sandstone I shall, therefore, waaR hesitation, refer to it ¢
the Potsdam sandstone.® vet

A list of fossils described in the memoir is given to citwetiate their
stratigraphic position.® In this list the fauna is divided into that oj f
the lower beds, middle beds, and upper beds, the latter characterized
especially by the presence of the genus Dikelocephalus. Ina supple
mentary note on the Potsdam sandstone that accompanies the memoir
he gives a résumé of the evidence upon which the lower sandstone o: ¢
the Upper Mississippi Valley has been placed in parallelism with th 7
sandstone of New York, known as the Potsdam sandstone, as follows:” ,

In comparing the older rocks of New York and of the East generally with those «

1 Physical geography and Rpnerat geology, Geol. Sury. Wisconsin, Report, vol. 1, 1862, p. 14. Sal
2Op. cit: , pp. 20-23. oe
3Stratigraphical geology. Geol. Surv. Wisconsin, Rep., vol. 1, 1862, pp. 140-144.
4Preliminary notice of the fauna of the Potsdam sandstone, with remarks on the previously kon
species of fossils ‘and descriptions of some new ones from the sandstone of the Upper Mississippi Val
ley. 16th Ann. Rep. Regents Univ. N. Y., State Cab. Nat. Hist. , 1863, pp. 119, 120.
5 Op. cit., p. 120. 3
8Op. cit., p. 209. 3 US Se an
-7Op. cit., pp. 211-213 Ree an

Sa eee | WISCONSIN. Le PCE

n outcrop of these maciine iia, between the St. Lawrence and the western
f Michigan on the Menomonee River, where we can expect little aid from
ology. The fossiliferous beds of these ancient formations in Wisconsin lie to

f hon, stretching southward from the region of Lake Superior far into the
neient The disconnection caused by this promontory between the East and
he eo West atta of itself prepare us to expect a fauna cdl in a great degree
beds of corresponding age on the opposite sides. _
= has been shown, by the investigations of the Canadian Survey, that not only the
ots dam sandstone, but all the fossiliferous beds below the Birdseye and Black River
imes ones are absent from Kingston on Lake Ontario to Lacloche on Lake Huron.
rom 1 Lacloche to Lake Superior there is a sandstone coming in below the Birdseye
estone, which, from its position, may be considered of the age of the Chazy! for-
ation and equivalent to the St. Peters sandstone of Wisconsin and Minnesota; and
a Bere rsadstone, doubtless, which has been taken for the Potsdam icaadocls in
e localities along that line.
a ‘The peucceeding Birdseye and Black River formation, from Lacloche to Lake Su-
, has become a buff-colored magnesian limestone, or weathering externally to
is color, but still holding the characteristic fossils.
a ew York a sandstone (the Potsdam) lies immediately beneath a magnesian
stone (the “ Calciferous sandrock”): this deposit is succeeded by a calcareous
ation (the Chazy), including a sandstone and surmounted by the Ryteaggic Black
r, and Trenton limestones.
ey weonein, Iowa, and Minnesota, we have undoubted Trenton limestone, and
v it a buff-colored magnesian limestone containing so many of the characteristic
ils of the Birdseye and Black River limestones as to leave no doubt of the paral-
Hi m of these beds with those of New York. Below this magnesian limestone we
re the St. Peters sandstone, corresponding, as already shown, with the Chazy for-
ati ion ; and beneath this a magnesian limestone, which, in its position and litholog-
sal « character, corresponds in all respects with the ‘ Caleiferees sandrock” of New

pe from all these facts that the lower sandstone of the Upper Mississippi Valley
en placed in 5 Taree with the sandstone of New York known as the “‘ Pots-

it may not yet be regarded as proved that the sandstone, from which I have
scril bed these fossils, is in all respects the equivalent of the Potsdam sandstone of
vied York, Vermont, and Canada. It may represent more, or it may represent less
‘that formation. The lower accessible beds of the Mississippi Valley may repre-
ent the Potsdam of 150 or 200 feet in thickness in the typical localities in New York,
hile the middle and upper beds of the West may be of epochs not represented in
erert of the series studied in New York; and in some other places, as in the re-

ons just mentioned, the same epochs may e represented by ashaly or semicalca-

ts * o ald not therefore be regarded as decided that the Potsdam sandstone, as devel-
ed in New York, occupies the entire interval from the base of the oldest sedimen-
ry formation of the Paleozic era to the Calciferous sandstone. From what we
1 of the primordial fauna in other localities, we are prepared to find beds above
w, or both above and below, the epoch represented (so far as now known) by
tsdam sandstone of New York, and which may still be of the same period.

“Chazy formation” of the Canadian Geological Survey, in its eastern localities, includes a
stone which comes in below the greater part of the limestone, leaving frum 10 to 20 feet of
wd limestone beneath (Geology of Canada, 1863, p.123). It is apparently this sandstone of the
formation, having i in Canada a thickness of 50 feet, which has become augmented in its west-
xte. ens on, while the calcareous part of the formation has partially or entirely disappeared.
- Eoli-61- 12
i 2% ae 74 2

ae .

4 . ao .-
ey : PaaS. > oe rey. £y ¥. 2 sy ~ px: z% Ves > fae .— aa wt : ic -
Pgs a See - tht Jeg i it? ° oe

us deposition, or may be included in the commencement of the Calciferous epoch. _

~

5

=

~~

_ sandstone, or the Chazy formation, will be found overlying the fossil-—

Se Si tae sie ne oe Be nt oe oe ERE 2 Ie pe ae ee
.§ > _ a ” —> a : E n>
eee. 08 Se Fe - ts - oa a aMe eS ene ens ean fs a ae - a7 > a i> G er ‘i
= mS ot Bec ae rie S, ter ae ace MAGS T ie a = tee a ee
D ly § e-cee ee BS es THE. CAMBRIAN. OS yt? S Se

~
:>

- this sandstone formation and that none of them are of teucons origin,

+S q = ; Je aa» Ee ' ee me +: * a pala

He ined enters upon the didousaion of the relative -age of the sand |
stones of Wisconsin and those of Lake Superior, and concludes that
‘while the older beds of the latter area are apparently below the foss! l--
iferous beds of the Upper Mississippi Valley, the newer sandstone _o ed
the St. Mary’s River, which is apparently of the age of. the St. Peter |

iferous sandstone, either with or without ie) intervention of the Lower n
Ma gnesian limestone.

On a geological map of Wisconsin published in 1855 Mr. I. A. Lapham é
- delineates the distribution of a sandstone occurring beneath the Lower
- Magnesian limestone. Under the same color he includes the sandstone”
on the south shore of Lake Superior, both on the north and southeastern |
side of the trap rocks of Keweenaw Point. The distribution of the
fossiliferous sandstone south and southeast and east of the northern
area of the primitive rocks is also laid down.? In a new geological
map of Wisconsin, published in 1869, only the sandstones of the north-—
western portion of the State are colored as Potsdam sandstone, In the.
vicinity of the shores of Lake Superior the Michigan area on the map 01 f
1855 is left uncolored. im

A paper onsthe age of the quartzites, schists, and conglomerates of
Sauk County, Wisconsin, by Prof. R. D. Irving, proves conclusivel; yo
that the quartzites are of pre-Potsdam age, and that the latter are ¢ de.
posited unconformably upon the flanks of the hill formed by the quate 7
ites.3 The evidence given by Prof. Irving negatives the conclusion ar
rived at by Dr. Alexander Winchell in his description of tke fossils ¢ f
Sauk County, where he states that Ptychaspis and Dikelocephalus
occur at the base of the Potsdam, and that the quartzites in quested D
are the lower beds of the Potsdam formation.’ In the region of south-
central Wisconsin, especially in Dane and Columbia Counties, Prof.
Irving obtained a thickness of 800 feet for the lower or Potsdam san d-
stone, and for the superjacent Mendota limestone 30 feet, above which
occurs the Madison sandstone, with a thickness of 35 feet, He referi
only the lower or Potsdam sandstone to the Primordial.® q

The sketch on the geology of northern Wisconsin by Mr. BE. T. ‘Swe ot
gives a general description of the Potsdam sandstone, and attention is 5
called to the fact that all the strata at the falls of St. Croix beiong to

is

as suggested by Dr. Owen.® vas

10p. cit., p. 220. ;
?Lapham, I. A.: Geological Map of Wisconsin. Milwaukee, 1855. Also a map for 1869. =
3 On the age of the quartzites, schists, and conglomerates of Sauk County, Wisconsin. Am. a v an
Sci., 3d ser., vol. 3, 1872, pp. 95-99. Wisc. Acad. Sci. Trans., vol. 1, 1872, pp. 129-137.
4 Notice of a small collection of fossils from the Potsdam sandstone of Wisconsin and the Ia ke
Superior sandstone of Michigan. Am. Jour. Sci., 2d ser., vol. 37, 1864, pp. 226-232. ry e
5 Note on some new points in the elementary stratification of the Primordial and Canadian rocks | of
south-central Wisconsin. Am. Jour. Sci., 3d ser., vol. 9, 1875, pp. 441, 443. bao
6Notes on the geology of northern Wisconsin. Wisc. Acad. Sci. Trans., vol. 3, 1876, p. 51.

Fe
a
Ze

ut tt r nde ee, SF shag pawn en aheintee oe as Sy it ce 2 ALS
Bios 7 wig ex ae By , sa 2 fs : s kita a) Sy ak aaa i
SRR gies, ey 797
pists: Ri ee ete "WISCONSIN. ete . 179. :

es ee Mispe ee ; . . 4

m and copper-bearing series; the horizontal beds of the former,
ayeith shells of SENOS lying directly upon the columar, mela-

hai aberlin contains a detailed account of the “ Potsdam sandstone?
Le Says:

The at itis the exact equivalent of the Potsdam sandstone of New York, as would
em to be implied by the name, is not absolutely certain, but as the term hasbeen =
ised to designate this formation in previous reports upon the geology of the State,

nd L as the weight of evidence and authority favors this view, the name Potsdam

ir Mistone will be used oo further hie iayseck in this prepare: 4

‘fossils found in the sandstone. The Madison sandstone and Men- .
a limestone are included as subdivisions of the terrane. ek
‘Re ference to the description of the Lower or “ Potsdam” sandstone

s of central Wisconsin by Prof. R. D. Irving,* will be made under.

he description of the Potsdam terrane in Wisconsin.

bs - general description of the mode of occurrence and character of the

: am sandstone in the lead regions of northwestern Wisconsin was

ou lished by Mr. Moses Strong in 1877.4

i Upon the basis-of work in St. Croix, Duun, and adjacent counties, —_— -
r. Tr. L. C. Wooster subdivided the ‘¢ Potsdam” as follows :>

i timbers indicate the distances below the Lower Magnesian aeons:
: a) Upper calcareous band: This varies greatly in thickness, and is the probable
rthwestern équivalent of the Mendota limestone near Madison; 75 to 85 feet.

i¢ (6) Lower calcareous band: The limestone characters and the thicken are more
mly persistent than in a; 14d to 195 feet.
Hudson trilobite beds: Quite rich in trilobites and brachiopods, including one
pecies of the former, with several undetermined ones; 150 to 200 feet.
¢ lauconite layers: These comprise those layers whi are very rich i in glauco-
nite. Crinoid stems were found in these at Hudson; 160 to 210 feet.

4 [ ab, c, and d, the lesser distance from the Lower Magnesian is true for western St.
y County, while the greater is nearer true for points east.

.e the age of the Crystalline rocks of Wisconsin. Am. Jour. Sci., 3d ser., vol. 13, 1877, p.

a of eat Wisedaaks) Geol. Wisc., Surv. of 1873-’77, tok, 2, 1877, p. 257.

ogy of central Wisconsin.) Geol. Wisc., Surv. of 1873-’77, vol. 2, 1877, pp. 525-607. mS
Wise. Surv. of, 1873-’77, vol. 2, 1877, pp. 668-688.

in St. Croix, Dunn, and adjacent counties. Geol. Surv. Wisconsin, Ann. Rep. for 1877, 1878

- almost conglomerates; 680 feet.

BOS Meee THE CAMBRIAN. ahs Ley se ee far :

(e)_Eau Claire trilobite beds: These hold at. least seven species of trilobites, of
-which three are new, and a few brachiopods. These beds mark the lower limit of

calcareous matter in the formation; 450 feet. 3
(f) Eau Claire grit: These Tani mark the upper limit of the coarse sandatence” |

The mode of occurrence and character of the “ Potsdam” sandstowe 4
in the upper St. Croix district is described in great detail by Mr. Moses —
Strong.! In this he shows the unconformity between the “ Potsdam”
and the subjacent strata referred to the Keweenawan (Keweenaw)
series, and describes the various sections of the sandstone exposed.
The knowledge of the local details of the distribution and character of |
the “ Potsdam” sandstone of the Mississippi region north of the Wis- —
consin River was increased by him in 1882 by the publication of many
sections and descriptive details that will be used in a summary of our 5
knowledge of the Cambrian rocks of that region. 7

The “ Potsdam” terrane of the lower St. Croix district was described
by Mr. L. C. Wooster in’the same volume with the report of Mr. Strong.
This report also contains considerable data that will be referred to in
the description of the Cambrian rocks of the region.?

The geographic distribution of the “ Potsdam” sandstone and its re-
lation to the subjacent pre-Cambrian rocks and the superjacent magne-
sian limestone is shown with great accuracy upon the general geologi- 1
cal map of Wisconsin, published in 1881, and in the two sections at the
bottom of the sheet. 4q

A note by A. A. Young on the crystallized inde of the Potsdam ”
- sandstone of Wisconsin describes the manner in which the original
grains of the sandstone are surrounded by ieee envelopes 0!
quartz. ; ae

The summary of the geology of Wisconsin Sy “Prog, 1730: Chamber-
lin contains a description of the rocks of the “ Potsdam ” period. Thes eo
include the ‘ Potsdam” epoch, the Lower Magnesian epoch, and the
St. Peters epoch, in part. A general description of the formations, ac-
companied by an account of the life of each epoch, is followed by som
general observations upon the Cambrian age, to which the formations 1S
are referred. at

The occurrence of a conglomerate formed of bowlders from the trap
of the copper-bearing series in a matrix of sandstone that contains frag-
ments of Linguloid shells, apparently Lingulepis pinnaformis, is noted
by Mr. L. C. Wooster at a locality on the St. Croix River. From the
mode of occurrence of the conglomerate he concludes that it must have

cal

1Geology of the upper St. Croix district. Geology of Wisconsin, survey of 1873-1879, 1880, vol. 3, p D.
39 0-428. ..

2(Geology of the Mississippi region north of the Wisconsin River. ] Geol. Wisconsin, survey of
187379, vol. 4, 1882, pp. 38-91.

3 [Geology of the lower St. Croix district.] Geol. Wisconsin, survey of 1873-79, vol. 4, 1882; pp. . 100
130.

4¥Further observations on the crystallized sands of the Potsdam sandstone of Wisconsin. Am. Jou
Sci., 3d ser., vol. 24, 1882, pp. 47-49. :

5General Geology. Geol. Wisconsin, survey of 1873-"79, vol. 1, 1883, pp. 119-200. > i

3 q ee
; Lise. ~

‘ k
’ * Soe = . i.
By is ear ty Ne,
a+ we nF
- > , « r
a ~*~ =>

i+

. —, vege | a - a ee a] oo? eer oO Ve at Sete ek) a Se ey > «ud Se See
of, SO Ape Bo ee Pe 2s PASH Si Wie eh alle ot ane as :
eT eS eer as ae. a =X pe ’
5 ES Sf nag igen : . 3
en J vs ve a ‘

po”. ae

4 ilated Se a | cliff of the copper-bearing rocks and that the age
he e conglomerate must be late “ Potsdam.”!
an extended paper on the classification of early Cambrian and

ween the “ Potsdam” EES and the Ba binoatrt Huronian and
K weenawan rocks. He also discusses the similar stratigraphic rela-
ns of the peti and pre-Cambrian rocks of the Grand Canon

“>
-

MINNESOTA.

below the Falls of St. Anthony to the Iowa line was proved by the
su vey of Dr. D. D. Owen in Wisconsin, Lowa, and Minnesota. Alter-

ae in

there is also a narrow area colored Potsdam along the valley of the
a
Minnesota or St. Peter’s River.

irvey of Minnesota, discussed, under the title of “‘ Potsdam Sandstone,”

‘ a idstone,” the fossiliferous sandstone of the southeastern portion of
t EeBtate, referred to the Potsdam by Dr. Owen.* Of the term “ Pots-
dam,” he says:

e?
‘This term is strictly applicable only to the sandstones of New York State, to whisk
7 Bessie was first given, and to the equivalents of those strata in their extension
ugh the West. It has been abundantly proved that the red sandstones of Lake
rior, however disturbed and changed locally, or however much increased in

kness by the agency of volcanic outbursts, are the exact equivalents of the New

or am rocks on which they lie unconformably,and from which they differ in being
mt slightly and only locally metamorphosed. They retain usually their ovidbatty
3 sedimentary characters, and have not well preserved fossil remains.®

agit He states further that in Wisconsin the upper sandstones are found
lie unconformably upon the red sandstones where they have been
it ed by voleanic agency, thus referring the quartzite of Sauk County
50 ay Potsdam, and the sh wee fossiliferous, Upper Cambrian

| fp Moik, to his St. Croix Sia The red sandstone or Sioux
rtz ite is said to be both older than and unconformable with the

n sition from the copper-bearing series to the Potsdam. Am. Jour. Sci., 3d ser., vol. 27, 1884, pp.

hh Dnthe classifi cation of the early Cambrian ang pre-Cambrian formations. U.S. Geol. Surv., 7th Ann
sp. for 1885-’ 86, 1888, pp. 365-454.

1852, pp. 48, 49.
eneral sketch of the geology of Minnesota. Geol. and b3, at. Hist. Survey Minnesota, 1st Ann. Rep.
B72 44 Ist ed., pp. 68-80.

ae aes x oes MINNESOTA. ay eo is &

ee Tl ne , presence of the lower siudgtoue along the Mississippi River.

st nating exposures of the strata occur along the river and some of the —
tributaries flowing into it from the west.2 On the accompanying map

: Dimas additional information in regard to Minnesota was published
until Prof. N. H. Winchell, in the first annual report of the geological —

Sioux quartzite of atGhereataen Minnesota, and “The St. Croix —

: Potsdam. They occupy the first position over the metamorphic slates of the Hu-

1. Surv. of Wis., Iowa, and Minn., and copeamsre aera of a portion of Nebraska Territory, Phila-

rd

7.

are eT Ae . “THE _CAMBRTAN. ae S a oe See “7

to the latter. oe

7

< - stone, of handsomely rounded quartzose grains.

- acquire a thickness, including the intercalated beds of shale, of shouns 600 feetin the; eir

~ ~ - x

of the ipper Mississippi, below the ewes Magnesian limestone, z
the Sioux quartzite he says that— ; Bis --

Its features here are easily identifiable with those of the Potsdam at the rapids in '
the St. Mary’s River, at Sault Ste. Marie, Michigan. In their passage to the west, the
over-lying, light-colored saudstones seem to become more largely developed. They

exposures along the Mississippi River. !

Of the fossils collected from the horizontal beds at the Falls = the St

Croix it is sage they: ae

to a ne izon much lower than that of the Lingula Beds of the Potsdam of New
York. The name has been still further removed from its original use by the Iow
geologists, in its application only to these upper beds, and in giving the name pea
quartzite to the western representative of the original Potsdam. Dr. Owen, althong
he recognized many points of difference between the Lake Superior and New
York Potsdam, and these light-colored sandstones of the St. Croix and Upper Missi s-
sippi, seems not to have noted the important fact that the former are everywhere sub-
ject to distortions and fractures by volcanic forces, while the latter are never known
to be disturbed by such causes. Itis true that he embraces both’ the red and the
‘light-colored sandstones in the designation of ‘‘ Potsdam,” and argues at length to
prove the great age of the red. (Geological Survey of Wisconsin, Teen and Minne: B=
sota, p. 187.) ~ a
It isin accord with geological inecestent: therefore, to separate these two sandstor J
formations under different names, retaining the name of Potsdam for the older, a d
giving provisionally the name of the St. Croix River, on which they are best expos sed,
_ The following reasons may be assigned: =
(1) The Potsdam beds were laid down before the close of the volcanic disturbaneem
evident in the rocks of the early Silurian and pre-Silurian ages; the St. Croix hb sa
were deposited and still lie in horizontal layers, cnceoloenas not only over t he
Latrentian and latest trappean rocks of the northwest, but also on the ops
beds of the Potsdam.?

(2) This reason has little péatitie and will not be quoted.

(3) The lithological characters of the Potsdam beds are uniformly different.
those of the St. Croix beds. The former are hard and often vitreous, usually Bh
brick-red color. Their bedding is very distinct, and often separated into slaty laye
by partings of red shale. They are strongly marked by the so-called fucoidal im
pressions. They are frequently ripple-marked and sun-cracked. The latter ar

white or butf-colored, often friable, and constitute a heavy bedded or massive t

(4) This notes differences in chemical composition. . a
(6) °The Potsdam sandstone has a thickness of at least bts feet ; (Note—D. ( ve

~ See Owen’s report on Wisconsin, Iowa, and Minnesota, p. 193); the St. Croix cial
also has a thickness of over 500 feet. It is more in keeping with the canons of
logical nomenclature to give separate titles to formations so well defined and : so
developed.

(7) This gives the evidence of paleontologic direc He's
that the fossils of the Potsdam sandstone of New York are Li

‘Op. cit., p. 69. 2 Op. ole pp- 69, 70. _* 5th does not occur in the or

antiqua (Con.) and Lingula prima (Con. ),a@ Disema (or Orbicula), and
u rtain i impressions supposed to be of a Pleurotomaria and of crin-
oidal remains. _A species of Theca has also been described from Keese-
‘lle. In comparison to this he cites a large number of species de-

s ser ibed by Owén and Hall from Wisconsin.!

> district and from the New York district, in the sandstone referred: by
’ im to the Potsdam sandstone, are the same, namely three.

~~

‘Notwithstanding these considerations, it has not been thought best to attempt the
delineation of the areas of these sandstones sir sgugse on the preliminary geological
nap accompanying this report.®

eo.

= i detailed description of the litiological character's of the St. Croix
nd Potsdam sandstone is also given.®

The preceding observations by Prof. Winchell have been ae in
‘ Sie letail as they are the foundation for the theoretical views subsequently
* eed by him correlating the Potsdam sandstone of New York with
rious other sandstones of pre-Silurian age.

On the map accompanying the report (opposite p. 45) the Sioux fiakeh
if it e area of northwestern Minnesota is colored the same as the St. Croix
‘y sandstone of the southeastern portion of the State. In the legend the
: color i is placed under the heading of Potsdam and St. Croix. .

In the fourth annual report Prof. Winchell describes the St. Croix sand-
5 0 ne as it occurs in Fillmore County and illustrates the geographic
is ribution on an accompanying map.* In some notes on a deep
well drilled at Minneapolis, Minnesota, the same writer states that Nos.
‘A, 12, and 13 represent the St. Croix sandstone with a total thickness
01 £217 feet. Beneath this there isa red marl and red sandstone which he
| refers to the same horizon as the catlinite beds of’ the Sioux quartzite
a es. Of No. 14 it is said: ‘No. 14 may represent the Lingula flags
r the upper portion of the Potsdam, so called.” No. 15 1s correlated
Bis Gudoubtedly the upper portion of the great series of marls and sands
which characterize this horizon in Minnesota. ‘It is the same forma-
tion as the rock that embraces the well known ‘pipestone’ or catlinite
of f Minnesota.” . :

_ The Sioux quartzite is referred by Prof. Winchell to the Potsdam
zndstone in adescription of the geology of rocks in Pipestone County -
in in the sixth annual report. Itincludes the famous pipestone quarry near
tl the center of Pipestone County.®
a more extended_account of the strata referred to the “‘ Potsdam ”
S sandstone is published by Prof. Winchell in the tenth annual report

pa:
C

a 1 Op p. cit., p. 71. 2 Op. cit,, p. 73. 8 Op. cit., pp. 75-80. r

Xe eport on the geology of Fillmore County. Geol. and Nat. Hist. Surv., Minnesota; 4th Ann. Rep.
1875, 1876, pp. 31-32.

S lotes on the deep well drilled at East Minneapolis, Minnesota, in 1874-’75. Minn. Acad. Sci.,

Bail; , vol. 1, 1876, pp. 188-189. Y

+ i ne geology of Rock and Pipestone Docamtles Geol.and Nat. Hist. Survey, Minnesota, 6th Ann.
eee, Vir p. 97. ~

2 (8) in this it is shown that the number of species of the Lake Superior |

.

=

x

a

& Pane” - ASE. © ea) 2 eo “~e we eet ee TO ee Se ee ae ~~, er St eat ‘he ee a .
TS MRE ES CREE AES Sng em ae ee ce ne en
, : . ay Sas oF gt tw, < te é .s wn as ., Sas <= . exes : oe y y-* os + ‘ R js A ie are 4
ws 2 ° a , — ee Ree eR as te oe tee 7s Fl oe ee "a yf
; = a » 24 Ww Of > ae sn ‘. + tees oe Fi : ar
4 . ’ a é = . “ ’ “ pe eet : = bs St S's a oe P. 5 er . 2 | a c ‘4
Sd Se he ete te ee
roo. eee : jew n ee PON ei, ae
- - ad a ‘3 ~ “Pe Q7
184 PES. THE CAMBRIAN. — OPS,

_ of the survey. In this he affirms that the horizontal fossiliferous be eds
referred to the Potsdam by Dr. Owen, Prof. Hall, and other authors is i
above the trne Potsdam of New York, and that the latter is reprotontay od d
by the rocks of the copper-bearing series in the west ;_ also, that no f
-sils representing the Primordial fauna have yet been discovered i in th fs
west nor have any been found in the western representative of the Pots-
dam; and finally, that the second fauna of Barrande is found in the
Gusbed group of Canada and in the St. Croix sandstone of the west,
lying in each case above the Potsdam sandstone.) a

An article by Dr. J. H. Kioos, translated by Prof. Winchell, describe oS
the rocks of the Falls of St. Anthony and the St. Croix River, and give aS
a description and a diagrammatic section of the river bank at Taylor’s
Falls, illustrating an unconformity between the Potsdam sandstone and
the subjacent copper- bearing rocks.” SS

In an account of the geology of a deep well drilled at Minneapolis t
- Prof. Winchell states that the drill passed through sandstone in the
lower portion of the well as indicated in the following section 33 ;

‘ Feet.
2 WDDEih Sos J odae Sob sutuantn eh ubmbates een i castes eet sckeee 10
2. Trenton limestone ..... 2)... Sa sece cee ees 5 DEg. Jem vues 24
3. Light, crumbling sandstone (St. Peter?) ............-.-... 125
4. Brown-red pipestone clay... 21... -.2. .--se2 --ee ee cee eceeee 2
6, Potedam gand..2 m9 -s0cusncc de tee encase oes cemees eae aca 42 |
6: Red quariaite;: Potsdam (s.200 032.2 Sone be endo eon 2 ee 102
7. Light-colored Potsdam sand and shales..--.....- oS dns 722
8. Red Potsdam sandstone and shales at least.......... eacdbe 347
1, 374

-- Particular attention is called to the brown-red pipestone clay of the
section, which is the equivalent of No. 12 of that section on page 212.
No. 6 of the section quoted is compared to a layer of red quartzite, seen
at New Ulm, Minnesota, and at pears Wisconsin. Commenting
upon this he says: : a

Thus we find an interbedded red quartzite in the Potsdam formation similar to
those seen in the same formation in the Buck Hills and in several other placed a
the Rocky Mountain region.* a

Attention is called to this statement as it is a correlation of a qua ta
ite of the Upper Cambrian rocks cf the Black Hills with a bed of

quartzite in the Sioux quartzite series of Minnesota and the Baraboo
_ quartzite series of Wisconsin. : : a |

In a tabulation of the strata beneath the lower fossiliferous sand-

tThe Potsdam Sandstone. Geol. and Nat. Hist. Survey Minnesota, 10th Aa ‘Rep. for 1881, 1 18.
p. 136. ;
2 Geological notes on Minnesota. (Translated by N.H. Winchell.) Geol. and Nat. Hist. Su: :
Minnesota, 10th Ann. Rep. for 1881, 1882, pp. 186-200. =

3 The geology of the deep well drilled by C. C. Whelpley at iuGikienpolis. at the *C” Washburn M fill.
Geol. and Nat. Hist. Survey Minnesota, 10th Ann. Rep. for 1881, 1882, p. 217. :

4Op. cit., p. 214. : ae

ne or St. Croix seailnaaie, Prof. N. H. Winchell defines the Pots-
n formation as follows: }

: sa ne

e - Potsdam formation. —Tilted red sandstones, shales and conglomerates, changed by

ig neous gabbros and dolerites locally to red quartzites, felsites, quartz-porphyries
nd to red granite. The Keweenian and Huronian in part, in Wisconsin.

pe » He places the Taconic group second and defines it as follows:
_ Taconic group.—Horizontal black slates and gray quartzites, with interbedded

_ ores, and silicious marble. The Gunflint beds, the Mesabi iron rocks, the

> Ogishke Muncie conglomer ate (?), the Thomson slates and quartzites, the Vermilion
in on rocks; the Huronian in part, in Wisconsin and Michigan.

4 a: description of the Sioux quartzite as it occurs at New Ulm is
given by Prof. Winchell in the second annual report.? In the first vol-
_ of the final report of the Minnesota survey he describes the St.

Croix sandstone as it occurs in Houston, Winona, and Fillmore Counties.?

The entire thickness of the fo1mation in Winona varies from 488 to 553
- feet. Under the title of Potsdam quartzite a description is given in
a volume by Messrs. Winchell and Upham of the pre-Cambrian
nartzite of northwestern Minnesota.°

Pom the Sioux quartzite series at Pipestone, Minnesota, Prof. .
“Winchell described, in 1885, Lingula calumet and Paradowides barberi,
Y ork.§ -

- Inanote on the revision of the stratigraphy of the Cambrian in
XN finnesota, Prof. Winchell includes under the St. Croix terrane, Jordan
sandstone, St. Lawrence limestone, shales, and Dresbach sandrock.’
Iti is interesting to note that after the upper member of the St. Croix,
the Jordan sandstone, we find “ Potsdam” (?); also after the Dresbach
8 andstone at the base and (Potsdam) after formations placed as pre-
St. Croix. - ;

1 Dakota and Minnesota is discussed by Prof. R. D. Irving,’ who con-
Sy ides that their tilted position, great thickness, and lithological con-

ool

me 2 ely a downward continuation of that formation, but, on the con-
tra ry, form a great uuconformably underlying series.”

8 OD the age of the rocks of the Mesabi and Vermilion iron districts. Geol.and Nat. Hist.,
4 ey Minnesota, 11th Ann. Rep. for 1883, 1884, p. 170.
_*The geology of the Minnesuta Valley. Geol. and Nat. Hist. Surv., Minn. 2d Ann. Rep. for1873, 1874,
aS

te The Geology of Minnesota. Vol.1, of the Final Report, 1884, pp. 223-227, 257-259.
_ 40p. p. Cit., p. 258.
_ 5Op. cit. pp. 422-424, 199-503.
For sils from the red quartzite at Pipestone! Geol. and Nat. Hist. Sarv. Minnesota, 13th Ann. Rep.
884, 1885, pp. 65-72.
Re Revision of the stratigraphy of the Cambrian in Minnesota. Geol. and Nat. Hist. Survey Minne-
4th Ann. Rep. for 1885, 1886, p. 337 p
eliminary paper on an Investigation of the Archean formations of the Northwestern sagen: U.
il. Surv. (i a -» 1883-84, 1885, pp. 201, 202.

Ne : r
: = ana . " a

sstones and diorites (the Animikié group), changed to tilted slates, quartzites, -

eS hs MINNESOTA, Se PGs 185

referring them to the ghd vahant of the Potsdam sandstone of New

ae _ The geological age of the Sioux quartzite of the pipestone quarries

tras st with the Potsdam sandstone ‘‘ make it evident that they are not |

upper portion of the St. Croix River.’ =a

called Potsdam of the Northwest, enters a series of dark red and brown shales a

; Re anatlo mides horizon) which apparently overlies the ‘‘ Animike.”” —

as * Typical Potsdam quartzite,” but he mentions no reasons for conclud- .

account of the geology of Goodhue’County he describes the formation

_ seribed by Mr. G. F. Matthew’ he considers the Taconic (Lower |

PARSING ERS REE Eo ae C8 pe pe ee
z re : < E te. Fg - ve: 4 ye ee tN
wt — yt poe Fond “s a ns ce | ier y= apes y= ee “yt Sk
; r ne Are Sie kee =
i eee He ‘THE “CAMBRIAN.. Se Pee “eas

4 : # mm es

Mr. Warren Cake in notes ou the geology of Minnehaha Conus ‘ss
Dakota,! refers to the rocks in various portions of Minn ehaha County

ing it to be of this age. No fossils were foundinit. ~ = aa
- In the second volume of the Geology of Minnesota Prof. N. H. Win 1
chell states that the St. Croix formation in Wabasha County is about

259 or 300 feet in thickness; and it is not known to vary particularl ly
in its stratigraphic composition from that of Winona County.? In the

and accompanies it with a list of the fossils found in the St. Croix
formation in the Upper Mississippi Valley.® .

In the same volume Mr. Warren Upham describes the St. Croix sand-
stone as it occurs in Chisago County,in the valley of the St. Croix River.
He also describes the formation as it occurs in Pine County, along the

In an article on the age of the St. Croix sandstone, Prof. N.
Winchell discusses its relations to the typical Potsdam of New Yor ork
and concludes it is a distinct formation.* In an account of a deep nod
drilled at Stillwater, Minnesota, it is poet by Mr. A. ay Meads that.

of drift, white friable sandstone, and green shales belonging to the St. Croix : and 60

brown feldspathic sandstones which exhibited a thickness of more than 1,500 fe
These gradually assume characters of a volcanic detrital tuffi—‘‘ amygdaloidal aa cal. -
citic, kaolinic, still brown, slightly siliceous—and finally at the depth of about 32 00
feet unmistakable beds of trap rock were encountered, alternating with sandst
beds. At this depth some grains of native copper were seen in the drillings,”

Prof. N. H. Winchell has recently published his latest conclusions : n
the Taconic rocks of Minnesota. On the evidence of the tracks de-

S: 4

brian) age of the ‘“ Animike” formation to be sufficiently established,

and thinks the name Taconic should be substituted for Animike.? — he D
Pewabic quartzite is referred to the base of the “ Animike,” although he h
says: “it was at first supposed to be the equivalent of the Potsdan Bes ;:

A correction is made in relation to the reference of the stratigraphic
position of the Granular quartz as follows :4 | or a

_ 1 Notes on the geology of Minnehaha County, Dakota. Geol. and Nat. Hist. Survey, Minnesota, st | Ma
Ann. Rep. for 1884, 1885, pp. 88-97. ‘
2The Geology of Minnesota, Vol.2 of Final Report, 1888, p. 13,
3 Op. cit., pp. 31-36.
4 The Geology of Minnesota. Vol. 2, Final Report, 1888, pp. 407, 409.
5Op. cit., pp. 637-642. :
6Geol.and Nat. Hist, Surv. of Minn., 17th Ann. Rep. for 1888, 1889, pp. 56-64.
? The Stillwater Deep Well: American Geologist, vol. 3, 1889, p. 342.
8 Am. Jour. Sci., 3d ser., vol. 39, 1890, p. 145.
®°The iron ores of Minnessta: - Geol. and Nat. Hist. Surv. Minnesota. Bull. No. 6, 1891, p. Vt
10 Op. cit., p. 125.
1 Qp. cit. Foot note on pp. 417, 418,

~

, years ago (“A Great Primordial Quartzyte,” vol. 1, p. 178), that the granular

tz probably overlies the black slate of the Taconic system, and is equivalent of
3 oi Red sandrock of Vermont. The Red sandrock appears to be a part and near the
oe the ‘‘Georgia series” and above the Winooski marble, but the ‘‘ granular

tz” lies below the Winooski marble. The typical Potsdam is probably the
ee ae anular’ quartz. ” But the Red sandrock, and also some light-colored, loose sand-
& at ones still higher have very largely been regarded its equivalent.

"22a
: ¥

ee IOWA.

On the map accompanying Dr. D. D. Owen’s report of the geological
“survey of Wisconsin, Iowa, and Minnesota a small area is colored as the
‘Potsdam sandstone of New York, in the northeastern corner of the
State!
x As State geologist of Iowa, Prof. J. Hall stated that the Potsdam-
“$e andstone attains its greatest exposures in Minnesota.and Wisconsin
a orth of the limits of Iowa, and about the regions of Lake Fepin. The
excavation of the Upper Iowa River, however, has removed the cal-
¢ erous sandstone; so that at the junction of that river with the Missis-
8h opi there is Se posail a broad belt of the lower rock. A general de-
‘8 C2 ‘iption of the sandstone is given with the statement that some slightly
rs jcareous bands contain fragments of trilobites. In numerous locali-
‘ shells of Lingula are found, though by no means so abundantly as
the same rocks in Minnesota. These fossiliferous bands appear in
p e vicinity of Lansing.” In the same volume there is a general ac.
count ofthe Potsdam or inferior sandstone by Prof. J. D. Whitney.’
ith a general description of the geology of lowa Dr. CO. A. White de-
“se cribes the Sioux quartzite as occurring in the extreme northwestern
co mer of the State. In the table of classification he places it as Hu-
ronian (?) and beneath the Potsdam sandstone.‘ This is the quartzite
ferred to the Potsdam in Minnesota by Prof. N. H. Winchell. In
5 ribing the Potsdam sandstone Dr. White states that it reaches a
known thickness in Iowa of 200 feet, and it is exposed only in a small
"i portion of the northeastern corner of the State.°®
ts In the account of a deep well at Emmetsburg, Iowa, Prof. N. H. Win-
1 a refers to a white sandstone found beneath the blue shales of ca

re

_ Philad elphia, 1852.
. Geology of Iowa, vol. 1, 1858, pp. 47-48.
3 betea, pp. 328-331.
‘General geology. Azoic, Lower Silurian, UpperSiluiiaa, and Devonian systems. Geol. Surv. lowa
Re » p. 168.
; p. cit., p. 172. : —_
setion of a deep well at Bmmetsburg, Iowa. Minn. Acad. Sci. Bull., vol. 1, 1880, pp. 387, 388.

ot
» »

a = ne

188 = PRECAMBRIAN. bs x eck

In deaetibin g a deep well at Washin eton, i in southeastern Towa, Prof,
S. Calvin states that a gray sandstone 1,230 feet from the surface prolg
ably represents the upper part of the Potsdam series$ > _

LAKE SUPERIOR SANDSTONE. 4 J

In an account of a journey along the south shore of Lake Superio: *
Dr. J. J. Bigsby describes a red and white sandstone, for the most part
horizontal, that predominates along the shore, resting in places on .
_ granite.? He also mentions the red sandstone of Point Keewawoona

and the sandrock described to him by Mr. Thomson.’
| The description of the geology of Lake Superior, by Capt. H. Ww.

Bayfield, mentions a horizontally stratified sandstone that he traced 3
from one extremity of the lake to the other, on both the north and _
south shores, and on many of the islands in the lake.. A description
of the mode of occurrence of the sandstone on the south shore of. the
lake is given, with several diagrams illustrating the unconformity be-
tween the granite and the sandstone.* He considers it quite probable
that the formation extended to the west and southwest as far as ‘the
foot of the Rocky Mountains, and that it might possibly be the same
as the sandstone at the Falls of Niagara, ete., but concluded it required
much more elaborate investigation than has yet been bestowed to ren-
der it certain that the sandstone of Lake Superior and that of the
extensive tracts of country mentioned are the same formation. He
then gives reasons for terming the sandstone of Lake Superior the Old a

Red. These are its position immediately on the granite, its structure, ‘

and component parts. No fossils were observed. The student will 1

find in this paper of Capt. Bayfield’s a very fair description of the sand. 7

stones -as they occur about Lake Superior, and it is worth reading i

connection with the controversy in relation to their age. : a

As State geologist of Michigan Dr. Douglass Houghton - ropom d
upon the strata of the northern peninsula. In the second annual report
he says that ‘the Old Red sandstone” has been very much shattered by
the protrusion of trap rock through it.6 In his third report a more omg oy

tended account is given of the Lake Superior sandstone on the Ste

Marie River. The sandstone passes conformably beneath the super-
_ jacent limestone.?’ Of the bulk of the formation he says: ~ — 4 p

~ The Lake Superior sandstone in its easterly prolongation does not ‘attain a ver
great thickness, but in proceeding westerly this thickness is vastly increased, attaining
on the south shore of Lake Superior to several hundred feet, .

a

1 Notes on the formations passed through in boring the deep well at Wachlagion, Iowa. Americ an

Geologist, vol. 1, 1888, p. 30. *
2 Notes on the geography and geology of Lake Superior. Quart. Jour. Lit., Sci. and Arts (of the Roys yal

_ Inst. of Gt. Brit.) vol. 18, 1825, p. 33. ts

3 Op. cit., p. 260. . <
siveddinbe of the geology of Lake Heperion: Quebec Lit. and Hist. Soc. Trans., vol. 1, 1829, p. 17, fi

2 and 3, on plate. , *
5 Op. cit., p. 19. -
(Peninsula District.) Second annual report State geologist of Michigan, Detroit, 1839, p.14,
7 Third annual report State geologist of Michigan. House Reps. Document, No, 8, 1840, ple ;

pe

7

- =~ ert > De ot SSD pee YS Pade. 4 Pu PIs > re » a
e IR > f eRe grees - oe ae i Re ~ 4 ied | “ = 5 ee o
“3 yi co : aa Ry ‘ , Q ° : a? ae

— | LAKE ‘SUPERIOR SANDSTONE. | -

—h ‘

sils, 23 in » tot after a careful examination (several years ago) along its whole
of f outcrop, on the southerly shore of Lake Superior, I have never been able to
et in the rocks a sin gle contained fossil. .

The fourth report describes the “lower or red sandstone and shales”
s follows: :

- The red sandstone, with its accompanying red and gray shales, occupies a much
Jai ger extent of the country bordering upon Lake Superior than any other single rock
a group of rocks. It rests upon the primary and metamorphie rocks immediately
z° a i from Chocolate River; upon the conglomerate and mixed rocks from near Eagle
Ri ver, of Keweenaw Point, west to the head of Lake Superior; upon the primary

trap, metamorphic and conglomerate rocks of the north shore of the lake, and upon
th eee rock of Isle Royale. It is this rock which forms the basis of the
el plateaus or valleys occupying the spaces between the several ranges of hills
sou th from Lake Superior, and west from Chocolate River. In these last situations
this rock i is frequently seen undisturbed to surround the bases of isolated knobs of

able evidences of very great disturbance.*
a second bed of sandstone is described as the “upper or gray sate
8 stone, ” Upon the shore of Lake Superior, and extending from Point
iro quois to Grand Island, a sandstone occurs, differing widely in its
a appearance from that before described. This sandstone rests wncon-
* ‘southeast, while the latter dips very considerably to the north or
39 hwest.”3
_ sandy limerock rests conformably and immediately upon the upper
or gray sandstone. The tabulation of the rocks of the Upper Peninsula
ane follows :* : :

9. Tertiary clays and sands.
8. Upper limerock group (embracing as members the Diasimons Island
and Mackinaw limestones).

7. Lower lime rock and shales.
_. 6, Sandy or intermediate limestone.

Thickness.

_ §. Upper or gray sandstone, mean ...-.- i an eiaiaghe ent ME Rea feet.. 700
4, Lower or red sand rock and shales, extreme -........----- do... 6,500
3. Mixed conglomerate and sand rock, extreme ...-.....--.- do... 4,200

_ 2 Conglomerate rock, extreme...... ....-.----------------- do... 5,260

+=
A ‘detailed account of the red sandrock and shales is given on pages
37 7 to 41. This is followed by a description of the upper or gray sand
rock, « of which he says:

Th e only remaining rock which separates the red sandrock from the limestone lying
Be the south is a gray or brownish sandrock that is almost wholly composed of

prains of quartz, usually feebly cemented with calcareous matter. The composition
4 this Tock differs from that of the lower sand rock i in bein g more exclusively quartz,

3 BS ‘Metamorphic, trap, and primary rocks.

oe h that of the red BRE CE FONG, It has already been stated that the red sandrock of

—

Ins

a ia 1p. cit., p.15. | 3 Op. cit., p. 19.
“ih ‘Fourth Ann. Rep. State _geologiat of Michigan, 4Op. cit., p. 22.
oie 1841, pp- 18, 19. "

g) ‘anite, though when near to or in contact with knobs or [of] trap there are invari--

rmably upon the red sandstone, the former dipping gently to the south

~~

eee So Oe, ae ee ae ee ie aie Soe Se ee nn eg

__ itsline of cleavage is very irregular, frequently being opposed to the line of stratifi-
- gation over very considerable districts of country. Two indistinct species of facoides_

: ~w z <> « , . eB « “mn fate BS - SS ; 2 Rites
<¥ 2a oS 3 foe = at Se Pin = Meee 1; ‘
1900 ee CAMBRIAN. Es ee Se pe oe

~

fs Ss > -
a Se) ’

> ? > -

the south coast dips sogulerly wontbarty: while ne upper or gray mabdlpiois 3 lips

equally regularly south or southeasterly, in which respect the last-mentioned ro c I
conforms to the limestones resting upon it, while it a. itself upon the uptilted edge
of the red sandrock below.! : “ee

The upper sandrock, like the lower, abounds in pao defined ripple marks, and

were all the fossils noticed in connection with it. a
-I was unable to obtain any observations upon the thickness of ‘las upper sand roe “s
Sean were satisfactory, but from the imperfect observations which were obtained
was led to conclude that the average thickness as far westerly as the Pictured. Rockag
does not vary far from 700 feet. The upper sandrock, like the rocks before mentor
wedges out as far as we proceed in an easterly direction.? — 3

When presenting to the Boston Society of N atural History an ace
count of his visit to Lake Superior Prof. H. D. Rogers states that. he
discovered in the neighborhood of Chocolate and Carp Rivers the fol-
lowing conditions of stratification : : ee '

First, a group of rocks, the equivalents, undoubtedly, of the Primal sandstone ar c 1
Primal slate of Profs. W. B. Rogers and H. D. Rogers, denominated, in the nomen- |
clature of the New York survey, the Potsdam sandstone, and these rocks, highly in
clined, and traversed by parallel east and west axes. Secondly, upon the uptilte
edges of this earliest Paleozoic formation rests, in an unconformable position an 7
with a very gentle northern dip, the conglomerates and shales of the red sandstone
series. Specimens of the conglomerate were displayed, in which the pebbles. were
all from the older rocks. Mr. Rogers thought this fact of unconformable superpos sie
tion an almost conclusive proof of a post-Paleozoic date; and he proceeded to angue ©)
from various points of analogy between the red atone itself, its trappean dike
and their mineral associations, with similar components of the Mesozoic or ne wo
red sandstone of the Atlantic States, that the formation in question is of equivalent
age and origin with this last-named interesting group of rocks.® a

In his reconnaissance of the Chippewa land district of Wisconsin, | D
- D. D. Owen examined a portion of the shores of Lake Superior. — He
noted the red sandstone, its mode of occurrence, and character. | He
states that various views have been advanced by different writers re-
- garding the age of the red sandstone, marls, and conglomerates of Lak ke ;
Superior. Some authors have referred them to the date of the oldes
sandstones of the New York system; others believe them to be con-
temporaneous with the New Red sandstone of Great Britain and - the
bunter Sandstein of Germany. He further states: “4 .

Judging, however, from lithological and mineralogical character, there certainly y
is strong presumptive evidence that they were deposited subsequently to the Carbas -
iferous era. : *

He calls attention to the strong resemblance between them anda
formations above the Coal Measures, not only of the State, but of son mi
parts of Europe. . a
_ Ranging through Connecticut, New Jersey, Marylan4, and Virginia there are | red
sandstone and marly beds that are almost a Beamterpiek of some portion of the I
Superior formations, as well in aspect as in composition; like them, too, they are

1Op. cit., pp. 41, 42, 8/3 - ta a [

2 Op. cit., pp. 42, 43. 4 ni

2 On the mineralogy and geology of the south shore of Lake Superior. Sones Soc. N at, E ;
vol. 2, 1846, p.125, mae Bie

"4 M : a Nee
~ = —

ee oe a . ae = ; :
se 1 by ranges of intreabte pase with accompanying veins of copper. * * *
We eae detail a comparison between these formations and those of the North-

dstone were the same in 1 geologic age. After reviewing the and of
irrence and the relation of the sandstone to other rocks, especially
limestone from which a fragmeut of Pentamerus oblongus. was ob-
ned, indicating the upper member of the Niagara, New York series,
he Besnrcinitea. that the sandstone of Keweenaw Point was not of the
§ Jam series,but that it was most probably the New Red, or that sys-
m of sandstones which is regarded as such in New England.?

In their report of 1849 Messrs. Foster and Whitney color the accom-
anying map of Keweenaw Point so as to indicate that they consider
Be aaudstons and conglomerate superior to the trap series, forming
e base of the Silurian system. The same coloring and nomenclature
used on the pei of the district be: ween Mackinaw Bay and Choco-

3 «A the same volume, following the report by Foster and Whitney, is
ag eneral description of the region between Keweenaw Point and Mon-
treal River. The writer says the age of the sandstone of Lake Superior
coulc d not be determined by any evidence he had been able to collect.
It is entirely destitute of fossils, and lies directly upon granitic rocks.‘
Wh ether it is written by Mr. Foster or Prof. Whitney is not stated.

f Lake Superior as resting at the base of all the fossiliferous rocks.°
evidently considered the horizontally bedded sandstone at Kewee-

Point the same as the disturbed sandstone on the opposite side.
given n by Mr. W. A. Burt. In the same report Mr. Bela Hubbard
tes that the Red sandrock is the equivalent of the Potsdam red sand-
k of the New York reports, and that on the map the geographic dis-

a dest extension on the south side.

Epo rt of a geological reconnaissance of the Chippewa land district of Wisconsin ; and incidentally
part of Iowa and of the Minnesota Territory, 30th Congress, Ist sess., Senate Ex. Doc, No. a,
pp. 57-58.

e epor ;on the geological and mineralogical survey of the mineral lands of the United States in the
> of ~ Ex. Doe. No.5, House of Reps., 31st Congress, 1st sess., part 3, 1849, pp. 398, 399,

2 Ag ak a eee aces PA eS ge PB Tee ed Re a edrteg
eo =< TAKE SUPERIOR | SANDSTONE. 191

ution skirts the trap range on both sides, but media by far its”

he i
ei o
% ‘

in M r. J. W. Foster states that he is disposed to regard the sandstone

Full. descriptive details of the sandstones at Keweenaw Point are also

Re EN 6 PO a See ae aS at Noe he ae
ear poe ae eg RL ees =. oe ae
a > Ae ee ewer wer A. e uy a hi =
192 : THE CAMBRIAN. ENS ES te

its approach to the trap, however, it is found more or less tilted from its original —
_ horizontal position, and is. also very much altered by its contact with that igneous —

- sandstone and superjacent limestone. No attempt is made to differen- ~

- dam sandstone, the Calciferous sandstone, the Trenton limestone, ete.*

/

_ divided in 1845 under Houghton, House of Reps., Ex. Doc. No. 5, part 3, 1849, p. 840.

-sandrock of New York, Prof. Jules Marcou disputes their correlatic 2

_ It here lies in nearly horizontal biseee! though “at the coast a alight dip Saek ae a
observable, becoming more apparent as it approaches the basin of Portage Lake. In.

rock. The evidences both of the deposition of this extensive rock formation in calm —
‘and shallow waters and of the subsequent change induced in it by the trap rocks —
when in a fused or heated state are very important.!

In their report upon the copper region of Lake Superior, Messrs, 4
Foster and Whitney tabulate the stratified sedimentary rocks as fol- 4
lows:2 | *. :

I. Conglomerate. —Not strictly a sedimentary rock, but a dimeuid tuff.
Il. Inferior sandstone.—Potsdam sandstone. or

III. Compact or Lower Magnesian limestone. - ‘Valeitetvts sandstone, Chazy lime-_ 4
stone, B rd’s-eye and Black River limestone. ~

This table is followed by a detailed description of the congionstatll

tiate the horizontally bedded Red sandstone, of Keweenaw Point, from }
the banded sandstone that occurs on the western part of the Point.

Of the transition of the sandstone to the magnesian limestone they
Say: ; a
The sandstone, as we ascend from the lower strata to the higher, is found to be less
colored by the oxides of iron, and to take into its composition particles of lime until |
finally it passes into well characterized, compact, magnesian limestone. * * * |
We apply the term magnesian to this belt to define its lithological characters, although ;
the associated organic remains would see m to indicate the presence of several of the -
lower Silurian groups, whieh can not be recognized by litholoyical differences. ~

A notice of the work by Foster and Whitney in the copper district
was published in the American Journal‘of Science, 2d series, voles
12, 1851, pp. 222-239. ,

In a letter describing the Silurian terrane of Lake Superior, Messrs.
Foster and Whitney reaffirm their opinion that the standstones of Lake 2)
Superior are of the age of the Potsdam of the New York series, and”
that the section exhibits the Azoic system at the base, upon which rests
the conglomerate, formed of igneous rocks, and then in turn the Po S-

In commenting upon this statement of Messrs. Foster and bles
that the Lake Superior sandstones are of the same age as the Potsdé

and considers the formation as equivalent to the New Red sandstone, as aS
was stated by Prof. Jackson.®

ta ‘
1 General observations upon the geology and topography of the district south of Lake Superior, s su ib-

. 2Report on the geology and topography of a portion of the Lake Superior land district in the State,
of Michigan. Washington, 1850. Stratified and sedimentary rocks. Vol. 1, 1850, p. 99. .
8Qp. cit., p.117. a
4(Apercu de l’ensemble des Terrains Siluriens du lac Supérieur.) Bull. Soc, géol. France, 2° s6r i
vol. 8, 1850, p. 91.
5 Response & lettre de MM. Foster et Whitney sur le lac Supérieur. Bull. Soc. géol. France, 2 3 :
vol. 8, 1850, pp. 101-105.

eR

?

stone?" a a sandstone on the north shore, occurring in insulated
tches on the isthmus between Thunder and Black Bays. This sand-
ne attains, according to Logan,a thickness of at least 200 feet.? On
, south shore the sandstones of the northwestern side of Keweenaw
Point are considered to be of the same age as those on the south side
y of the point, extending along the lake shore from Keweenaw Bay to St.
Ty’s River. The sandstone extending southward, subparallel to the
bay, is also cor related with the sandstone mentioned; and all of these
correlated with the Potsdam sandstone of the are York series.
q ut 1ey quote from the manuscript of Prof. James Hall in relation to the
westward extension of the sandstone in Wisconsin, in the Upper Mis-
‘Si ssippi Valley.’
Tn some observations on the age of the sandstones of the United
Ste tes Prof. 0. T. Jackson concludes that the Lake Superior sandstone .
is of Upper Silurian age.‘
~ Messrs. Foster and Whitney returned to the discussion of the age of
the sandstone of Lake Superior in 1851 and conclude there can no longer —
be 2 any doubt that this sandstone lies below the lowest fossiliferous
T nem bers of the Silurian in the position of the Potsdam sandstone of
is ‘ew York. 5 They describe with considerable detail the mode of occur-
= ence of the horizontally bedded sandstone at the southeastern end of
the » lake along the Sault Ste. Marie, with its extension westward along
the coast to Keweenaw Bay. They show it to be one continuous for- |
ation around the great central granitic and azoie nucleus; that it is
a granal quartzose material, mostly friable, and containing little
ron; that the thickness of the aati formation did not exceed 100 feet
it xt Sault Ste. Marie, and that at the Pictured Rocks it was probably
more than 300 or 350 feet, gradually increasing from the east toward
west. 6 They then describe a sandstone on the western side of the
weenaw Point and Isle Royale which is now referred to the Algon-
m. This is the best résumé of the information relating to the Lake~
perior sandstone published up to its date.
n his tabulation of the lowest Protozoic sandstones Dr. D. D. Owen
aces: the Lake Superior ferruginous and argillaceous sandstones,
les, and-econglomerates at the base of the section, assigning it a

ckness of 5,000 feet.7 On the accompanying map the Lake Superior

€
oe

‘Lower Silurian System. Potsdam and Calciferous Sandstones. Rept. on Geol. of Lake Superior
i Distr., Pt. 2, 1851, pp. 113-134.

— 2Op. cit., p. 115.

409. cit., pp. 133, 134.

- 4{Some observations on the age of the sandstones of the United States.} Bost. Soc. Nat. Hist. Proc.,

13

POSS SPAS ‘THE CAMBRIAN.

sandstone west of the Montreal River pppan ree the same as the oan
stones of the central portion of Wisconsin referred to the Potsdam. - In rs
the legend the Lake Superior sandstone is included with the lower
sandstones of Wisconsin and Minnesota as the equivalent of the Pots-
dam sandstone of New York. oy
Mr. J. C. Norwood calls attention to the resemblance of the sandstone’
on the south shore of Lake Superior, west of Montreal River, to the
sandstones of the Chippewa, St. Croix, and Kettle Rivers... A section
is given that occurs above the mouth of Cranberry River.! .
In some remarks connected with the geology of the north shore of
Lake Superior Prof. J. D. Whitney states that from Sault Ste. Marie,
following the south shore in its whole extent, and along the north side ~
as far east as the northeastern extremity of Neepigon Bay, we find ex-
posed on the lake shore only shales, sandstones, and conglomerates,
the equivalent of the Potsdam sandstone and the accompanying trap:
pean rocks. 4
In speaking of the red sandstone of Lake Superior Mr. H. R. School!
craft states that in his expedition of 1820 he recognized ; a sandstone at
_ the Sault of St. Mary’s. He says: a |
That this is the Old Red sandstone may be inferred simply from the fact that, al- ag
though deposited originally in horizontal beds, its position has been disturbed in 3
many ‘localities,* 2
In his report as State geologist of Michigan Dr. A. Winchell describes aS
the sandstone at the Falls of the St. Mary’s River, where it has a
measured thickness of at least 18 feet. On some of the surfaces he ob:
served obscure traces of Algze. On some specimens from the Montreal
. River not less than three species of fossil plants have been discovered,
He favors the view that the sandstones of the south shore of oar Su-
perior are of the age of the Potsdam.‘ i
When commenting upon the fact that Prof. Jules Marcou had re-
ferred the red sandstone of Lake Superior to the Trias Prof. a3
Newberry states:
No American geologist will need to be informed that the sandstones of Lake Supe. -
rior are of the age of the Potsdam of New York and lie at the base of the Siluria 0
series. It is true that there is considerable lithological resemblance between ‘the
Potsdam sandstones of Lake Superior and those overlying the Carboniferous series it

New Mexico; but that fact serves simply to show how fallacious are > the inferences

derived lous from lithological characters.® : ;
— x5

1Description of the geology of middle and western Minn., including the country adjacent to tl the
northwest and part of the southwest shore of Lake ea nel Rep. Geol. Surv. of Wis., Towa, ai and
Minn., and, incidentally, of a portion of Nebraska Territory. Philadelphia, 1852, p. 269. -- ae

Remarks on some points connected with the geology of the north shore of Lake Superior. Am.
Assoc. Proc., vol. 9, 1855, p. 205. a

3 Observations on the geology and mineralogy of the region embracing the sources of the Mississip ppt
River and the Great Lake basins during the expedition of 1820. Schooleraft’s Mississippi Rin
Phila., 1855, pp. 316, 317.

4Geology, general sketch. Geol. Surv. Michigan, Ist Biennial Rep. of Prog. Lansing, 88.
49-51.

5 Geological report. Report upon the Colorado River of the West, ie in 1857-’58 by Lieut. J. be om
Part 11, 1861, p. 75. : oS

, eer ON ah ima we cia 9 cane aa *
, ae ‘ x ii Oe ‘i = ‘

oe K 3 yx : ; ’

: as Re LAKE SUPERIOR SANDSTONE. a GE

os A Bo Bsethetn rim of the great Paleozoic basin of North America the Potsdam
sandstone of the New York geologists is unquestionably the lowest rock from below
Qt ebec to the Island of Montreal, and thence passing up the valley of Lake Champlain
ae i sweeping round the Adirondack Mountains until it reenters Canada and soon dis-
pepeats to the north of Lake Ontario, where the Birdseye and Black River limestones
® directly upon the Laurentian rocks, and furthermore overlie the great Lake
Su Epsrior group of slates and sandstones, which, reposing on the unconformable Hu-
ronian system, constitute the upper copper-bearing rocks of. this region. This Lake
Superior group, as Sir William Logan remarks, may then include the Potsdam, Cal-
cai i erous, and Chazy, and thus be equivalent in part to the Quebec group, hereafter to
be e described. i 2
‘The section on the Montreal River, including 11,850 feet of strata,
according to Mr. Charles Whittlesey, is referred by him to the Potsdam
sandstone, with a statement that this is not the entire thickness of the
Potsdam at the mouth of the Montreal.? He states that some foreign
ge ologists have essayed to place this formation nearly at the summit
of the geological system, not only without evidence but against the most
co nclusive proof. He correlates the sandstone at the Falls of the St.
Jroix, with its abundance of fossils, with the sandstone of the section
™m tioned, and states that it has been traced stratigraphically beneath
‘the Trenton and Calciferous strata of the New York survey, on the
St. Mary’s River, at the Pictured Rocks, on the Escanawba, the Menom-
inee, Oconto, Wolf, Wisconsin, and St. Croix Rivers.
= The view that the sandstones and superjacent rocks of the south
shore of Lake Superior were deposited within the lake’s basin when
th 1e lake stood at a higher level has been held only, as far as known to
me e, by Mr. Thomas Macfarlane. In a report on the geological forma-
sions of Lake Superior he says:
z n the otherhand, the Upper rocks and St. Mary sandstones are never found far
and, but occur close to the shore in comparatively low-lying land and rocks. They

eem to have had, as the theater of their eruption and deposition, the bottom of the
Jal e, at a time when its surface was at a higher level than it is at present, although

= t so high as the general surface of the surrounding Laurentian and Huronian hills.4
‘In a paper on the position of the sandstone of the southern slope of
a portion of Keweenaw Point, Lake Superior, Prof. Alexander Agassiz
States that the sandstone of the southern side of the mineral range in
the % vicinity of Torch Lake is plainly of a differentage, lying, as it does,
une onformably upon the former (i. e., the trap). This view agrees with
t bat held by the geologists who refer the sandstone of the southern por-
‘tion of Keweenaw Point to the Potsdam, and that of the northern

Cc coast to a pre-Potsdam formation.®
a al
“100 some points in American geology. Am. Jour. Sci., 3d ser., , vol. 31, 1861, p. 397.
? The) Penokie Mineral Range, Wisconsin. Bost. Soc. N at. Hist. Proc., vol. 9, 1863, p. 238.
es Dp. cit., p. 239.
401 n the geological formation of Lake Superior. Canad. Naturalist, new ser., vol. 3, 1867, p.178.
¥ Ont he position of the sandstone of the southern slope of a portion of Keweenaw Point, Lake

Sa ior. Boston Soc. Nat. Hist., weka vol. 11, 186%, p, 245.

lor, Messrs. Brooks and Pumpelly refer the sandstones of the sou the

x rae oS ee ae 0 PA ee ee ean oe ee

5 BR es st ow fe Sh eye Po ia rah tay ee See

= +: x —3 a —— = te A x meee nt wh
: = < ¥) ; ~~ . FETS, 2 AL. ed Sa See” ee » Ane
. Gory aR 5 LE TET ES tam, Se
: - . . c : < ’ ~ ale Ose. - SS5 oa ae
L9G ee THE CAMBRIAN. . = #in =< oe
“~-

In an ariel on the age of the copper-bearing rioks of Lake Super a

shore to the Silurian, and state that they were deposited unconforma
bly upon the subjacent copper-bearing rocks.! a

In his report upon the Paleozoic rocks of Michigan, Dr. C. Romin. 7
ger concludes that the Lake Superior sandstone is the equivalent of the )
Potsdam sandstone. He states that there is no record of any instanem
in which recognizable fossils were found in situ in the Lake Superior
sandstone.?. The reference of the sandstones of the western side of
Keweenaw Point is based upon their lithologic resemblance to those
east of the trap range along the center of the point. 4

In a paper on some points in the geology of northern Wisconsin e
- Prof. R. D. Irving drew the conclusions that— - i

§

=

(1) The Copper-Bearing and Huronian series were once spread out horizontally
one over the other and owe their present highly tilted position to one and the same
disturbance. (2) That subsequently, after a long period of erosion, the horizontal
Silurian sandstones were laid down over and against the upturned edges of the
Copper-Bearing series, filling also the synclinal, in Ashland County, which lies De-
tween the northward and southward dipping sandstones. (3) That hence the Cop-
per-Bearing series is more clearly allied to the Archean than to the Silurian recks.3 —

He describes the series of horizontal sandstones and shales that form
the basement rock of the Apostle Islands and the north coast line a
_ Ashland, Bayfield, and Douglas Counties. These he considers in every
way to BS the equivalent, or, which is more probable, the downwaam 1
continuation of light-colored Primordial sandstone of the Mississip} pi
Valley. They reappear farther south, on the headwaters of the St.
Croix, from whence they can be traced uninterruptedly until they dis-
appear beneath the light-colored sandstones of the Mississippi Valley.*
This paper of Prof. Irving’s was reprinted in the American Journal of
Science, under the title ‘On the age of the copper-bearing rocks of £
Lake Superior,” ete.° ‘

It is stated-by Mr. E. T. Sweet that the term ‘ Lake Superior sand-
stone” “is generally employed to designate the reddish aluminou 1s
sandstones which nearly everywhere border the south shore of Lake
Superior. They also form the basement rock of the Apostle Islands,
They have never been found ina tilted condition.”® He considers tha at
Dr. Rominger, of the Michigan Geological Survey, has definitely set-
tled that these sandstones are the downward continuation of the light ;
colored sandstones of the Mississippi Valley;’ and concludes that t the
western sandstone of Irving, or thas of the Apostle Islands and vic sin-

=

1 On the age of the copper-bearing rocks of Lake Superior. Am. Jour. Sci., 3d ser., vol. 3, 1872, pp.

431-432. ae
2 Paleozoic rocks. Geol.Sury. Michigan, Upper Peninsula, 1869-1873, vol. 1, pt.3, 1873,p.80. ~
3On some points in the geology of northern Wisconsin. Wisconsin Acad. Sci. Trans. , vol, 2, 1874, p.

117. : 28 a
4 Op. cit., pp.114,115. | wie a
5Am. Jour. Sci., 3d ser., vol. 8, 1874, pp. 46-56. 4a
6 Notes on the geology of northern Wisconsin. Wis. Acad. Sci. Trans., , Vol, 3, 1876, p. 48.. e"
7 Op. cit., p. 49.

Se ae eS < 3 2 sis Pe i eee >, eee a. ee eS
al “4 > . be Peed a Paid .

=

(Re
Sx ig
Rg
ig
1

}

o
\
ad
A
|

e . Gast of Raweaiaw Point.

f A description of the Lake Superior eeiatans | is given by De Irving
n his account of the geological structure of northern Wisconsin that is
- fall and complete, and it will be referred to again in the summary
of our present knowledge of that formation.’ In the account of the
ge jeology of the eastern Lake Superior district in the same volume Dr.
Apostle Islands and adjoining shore.2 An account of the sandstone
s it occurs in the western Lake Superior district is given by Mr. E. T.
Sweet in 1880.3

€ _ Dr. M. E. Wadsworth notes that the sandstone at Marquette rests
npon the Azoic schists. That south of the Carp River, iu the locality
fig ured by Messrs. Foster and Whitney, the sandstone strata are seen
to abut against and overlie the vertical edges of the quartzite.‘

A eneral account of the Potsdam sandstone series is given by Dr.
R. D. Irving in his article on the mineral resources of Wisconsin. Of
the Lake Superior sandstone he says:

RK: ; The horizontal sandstone of the south shore of Lake Superior belongs unquestion-
ably y to this formation, though it is a matter of doubt whether the two sandstones do

sver did connect. The Lake Superior rock differs from its more southern equiva-
-in-its red color.®
“the sandstones at the eastern end of Lake Superior, on sie St. Mary’s
River, were referred to the Chazy formation by Sir W. E. Logan. Dr.
IS. Hunt calls this view a speculation, which was shown to be unten-
able by the establishment of the Potsdam age of the sandstones over-
lying the quartzites of Wisconsin and in northern Michigan, where
inger finds the upper sandstone to be overlaid by Calciferous-Chazy
beds.®
4 a Eastern sandstone, or that between the Keweenaw Ridge and
astward along the south shore of Lake Superior, is well described by
R. D. Irving in his account of the copper-bearing rocks of Lake
erior.’ This is followed by a description of the western sandstone,
O1 that occurring on the south shore of the lake, west of Keweenaw
Point. An abstract of this report also appeared in the third annual
feport of the U.S. Geological Survey, 1883, pp. 89-188.

ro
ar
a
a

24

rior Dr. A. R. C. Selwyn states that he considers the trap and
dstone to be of Lower Cambrian age. He calls them all Lower
nbrian, which includes Potsdam and Primordial Silurian. He holds

gers veo aaiirees of Wisconsin. Am. Inst. Mining Eng. Trans., vol. 8, 1880, p. 489.
Geology of Lake ee eo tas vol. 1, 1883, p. 219.

Ir ving described the Lake Superior or Potsdam sandstone of the

Bin an article on the age of the rocks ef the northern shore of Lake |

unconformity, a series of sandstones holding Cambrian fossils. * * -* (2) That ~

ve

det Pe SOG Te BOR TRENT EY ng I Sea NR ee a ay el aa
; ae “ AN deca ? . . . = we - hee ie Coe een Sey : ee > oes aero “ei 7 N
eyo a S . ae -." 1 wes - Pe » f »
¢ ‘ .

oh 3 ; wet o Soe A gd eae ee Fea
198 , | THE CAMBRIAN, 7 > fy. faUUR LG

that there is at present no evidence whatever on the north Bie of Lake.
Superior of their holding any other place in the geological series.' i

This view of Dr. Selwyn’s was concurred in by Prof. J. D. Whitney, —
who stated it to be the opinion held by Messrs. Foster and Natacha:
thirty years previously.”

Dr. Irving took exception to the statement made by Dr. Selwyn that
there is no evidence whatever of the rocks holding any other place in”
- the geological series than that including the Potsdam and Primordial »
Silurian, and stated: ; 3

(1) That the copper-bearing rocks underlie unconformably, and with an immense~

_ the copper-bearing strata also underlie unconformably the ‘eastern sandstone” of —
the south shore of the eastern half of Lake Superior. * * * (3) That the time- =
gap between the copper-bearing series and the Huronian was too long to allow of —
our classing them together.*

~The view of Messrs. Selwyn and Whitney was also opposed by Dr.
1. S. Hunt, who referred the basal sandstone to a pre-Cambrian group.*

Ina Hots on Dr. Selwyn’s paper, Prof. N. H. Winchell concurs with —
him in the sweeping affirmation that there is at present no evidence —
whatever of their (i. e., the copper-bearing rocks) holding any other place -
in the geological series than that of the Potsdam or Primordial Silurian. —
‘¢] would also add that there is incontestible evidence ee they can oles
no other.” ®

In opposition to the view of Prof. Winchell, Prof. Chamberlin stated |
the evidence upon which the pre-Cambrian age of the copper-bearing _
series of Lake Superior is based. It is (1) the general stratigraphical —
relation indicated. This he considers to be the weakest of all. (2)
Differences in thickness ; (3) differences in constitution ; (4) unconform-
ity ; (5) the inherent inconsistency of the view; (6) the dynamic sim- —
plicity of the view; (7) the discovery ofa like ae in the Grand Cafion —
of the Colorado.® | a

Shortly after Prof. Chamberlin’s paper, Dr. M. EK. Wadsworth pub-—
lished an article on the relations of the Keweenawan series to the Kast-
ern sandstones. His observations differ from those of Dr. Irving and
he claims that the Keweenawan series has no existence distinct from or
older than the sandstone of Potsdam age. In speaking of his observa-~
tions he says, ‘** These observations also prove at the birthplace of the
Keweenawan series, that formation and the Eastern sandstone were 4
one and the same.”

The paper of Dr. Wadsworth was followed shortly after by one. of
Messrs. Whitney and Wadsworth on the “Azoic system and its pro

1A ge of the rocks on the northern shore of Lake Superior. Science, vol. 1, 1883, PP- 11, 221.

2Geology of Lake Superior. Science, vol.1, 1883, p. 39. “ iy

3 The copper-bearing rocks of Lake Superior. Science, vol. 1, 1883, pp. 140, 141, 359, 360, 422. iS
4The Geology of Lake Superior. Science, vol. 1, 1883, pp. 218, 219. _ 3
5 The Lake Superior Rocks. Science, vol. 1, 1883, p. 334. ; ee
6 The copper-bearing series of Lake Superior. Science, vol. 1, 1883, pp. 453-455. a ae
7On the relation of the ‘‘ Keweenawan series”’ to the Eastern sandstone in the vicinity of Tore D
Lake, Michigan. Boston Soc. Nat. Hist. Proc., vol. 23, 1884, p. 1th. a PS “1
7) t

ae.

\ Se: a

ae Veep ah eee as deat ar eS? eee Mes ee he OE BU eG ee A ee oe ee 2 ee Pel
rs 4 “" ee gree oy; ag ee ~ Ae A Tt es ae i. “~ , . o .

4 7 eee < > ree “ip tie hs Nan: q, A's the Ss \ &, ¥ ee Sg at is oes spa a y

‘ Be age bite ee Sites ia > . Lt ee re . ; ;

‘ sf? aes se es . ae = = Se

Mey MISSOURI. TOM Eee keg 199

Se7 «
posed ibdtiviatons.” This saad a critical review of the published
pape ers upon the age of the enppcetinaring rocks of Michigan, Wisconsin, ~
é d Canada.!

au ae of Keweenaw Point, showing the distribution of the Eastern sand-
st ne to be confined to the southeastern side of the point, the northern
and northwestern sides being formed of the Keweenaw series.” They
: iscuss the views held by Messrs. Jackson, Foster and Whitney, Agas-
Siz, Rominger, and Creduer upon the stratigraphic position in the geo-
Ne 4 ogic Series of the Eastern sandstone and the sandstones of the Kewee-
nawan series ; and give also a detailed account of the contact between
‘the Se dagicne and the Keweenaw rocks.

MISSOURI.

oe The first notice we have of a sandstone about the Ozark Mountains of
southeastern Missouri is by Dr. Edwin James in 1822, who called atten-
tion to an inclined sandstone, like that of the Avephagy Mountains,
between which and the granite there intervened a stratum of clay-
7 slate highly inclined and resembling the primitive clay slate of New
ae F

c Ae This was followed twenty-nine years later by a sketch of the geology of —
the State of Missouri, in which Mr. H. King describes what he calls the.
second magnesian limestone. Beneath this is a sandstone which he
‘was inclined to correlate with the Potsdam sandstone of New York.
a The presence, however, of Lituites, Euomphalus, Pleurotomaria, Nat-
ica? was opposed to this view, but the stratigraphic and lithologic
‘evidence sustains the correlation. In order to explain the presence of
‘the fossils he suggests that “this may be an independent formation
“not represented in New York or elsewhere, and yet nearly contemporary
Wi th the first evidences of organic existence there and to be associated
Ww ith them in the same geological epoch.”

The work of the first Missouri survey proved the presence of four
: magnesian limestones with a belt of sandstone between the third and
the fourth, the fourth limestone forming the base of the series. Prof.
G . C. Swallow describes the third sandstone, above the fourth magne-
8 sian limestone, as a white saccharoidal sandstone, made up of slightly
ere transparent globular and angular particles of silex. It is as-
Ԥ sig ied a thickness of 30 feet, and owing to its position beiow the third
magnesian limestone is considered at least as old as the Calciferous
san ndrock, and there is great probability that it may prove to be beneath

ie
meu

2 *y The Azoic system and its proposed subdivisions. Harvard Mus. Comp. Zool. Bull., vol. 7, 1884, pp.
, 1297 98. —

€ 2Observations on the junction between the Eastern sandstone and the Keweenaw series on Keweenaw
Poi int, Lake Superior. U.S. Geol. Surv. Bull., No. 23, 1885, pl. i.

a * Geological sketches of the Mississippi Valley. Phil. Aead. Sci., Jour., vol. 2, 1822, p. 329.

«Some remarks on the geology of the State of Missouri. Am. Assoc. Proc., vol. 5, 1851, pp. 190, 191.

the tabulation of the strata as determined in Missouri both the third
__ Sandstone, and the fourth magnesian limestone are included under Cal i

2 ES a Lingula grit.” In this there were observed Lingulella lamborni,

1 nie, Fe eye FT ay ESS AY | Ra A es i ee oe ee ee ees Tee ee
’ ¥- ee ee AP ee eh eS : ge FS: Se ae a,
. ae + ‘es apt are Te, ee c eso <a Se 3
a 3 “Ate ST ee A ee ee
A > y x +. - = . fal ae a ee ; ie SE
Wav = . = | a Po re ee
200. > = a rds “THE CAMBRIAN. eae ee
i ; ifyr 2 ea

_ the Potsdam sandstone.! Th a 1 foot: note on page 129 it is said ‘shad

_ since the report was written Mr. Meek discovered. a trilobite in the third —
-magnesian limestone, which he and Dr. B. F. Shumard considered :
identical with one from the Potsdam sandstone of the Northwest. In

_ ciferous sandrock.?
When speaking of the geological map and the section of the rae of
Missouri, prepared prior to 1861, Prof. G. C. Swallow states that the |
Potsdam sandstone rests uneonformably upon the Azoic stratified ‘
slates of Missouri.? ia
The presence of the third sah aatains and the fourth magnesian lime- —
stone is noted by Mr. F. B. Meek in Morgan and Miller Counties. In-
Miller County the two formations have a thickness of 33 feet and in Mor- ©
gan County the third sandstone varies from 15 to 30 feet. The fourth —
magnesian limestone is assigned a thickness of 150 feet.‘
- On the map of Madison County, prepared by Messrs. C. J. Norwouin Be
and G. C. Broadhead, the geographic distribution of the- rake referred
to the Cambrian and pre-Cambrian is delineated. °
Below the third magnesian limestone in Madison, St. Francois, and
Iron Counties, Prof. G. C. Broadhead found siliceous or gritstone beds
with intercalated magnesian limestones and subjacent to these are ma “a
‘ble beds, beneath which occur sandstones, conglomerates, and shales.
These are numbered one, two, and three, respectively. In No.3, beneath
the third magnesian limestone, Lingulella lamborni, Meek occurs. On-
the St. Francois River, in Madison County, the lower unaltered sand-
stones rest directly on the granite. :
Ata deep well at the St. Louis County Insane Asylum ee following
section is referred to as beneath the third magnesian limestone:

; 11. 98 feet of third sandstone. :
12. 384 feet of fourth magnesian limestone. ~
13. 54 feet of Potsdam sandstone.
14, 245-4 feet, mostly granite, although a beniten of the upper
part may be sandstone. .
15. 40 feet of granite.’

A more detailed account of the strata beneath the third magnesiar n
limestone is given on pages 352-357. The fossiliferous bed is separa

<
a

1Geology of Missouri. Silurian eee Geol. Surv. (Missouri; 1st and 2d ann. repts , part,
1855, pp..128, 129.

2 Op. cit., pls. between pp. 60 and 61.

? Remarks on the Geological Map and Section of the rocks of Missouri. Am. Nat. ,vol.5, 1871, p.5

4 Reports on the geological survey of the State of Missouri, 1855-1871, 1873, pp. 127, 149. ‘a

5 Atlas accompanying Geological Survey of Missouri, Report,including field work of 1873-1874, %
vol. 1. Jefferson City, 1874. ~

6 Op. cit., p. 31. . “ Mie 0

7 Op. cit., p., 32. 2

re a a as +
“ a -
nd ri, Ae

tte genus Zaphrentis.

(1 sa lamborni and Seniithas should be found in the Calciferous
to No. 1, inclusive, as Calciferous.1. The marble of southeastern Mis-
souri was referred in 1882 by Prof. Broadhead to the older series or
. Potsdam, and the upper series to the Upper Silurian, with the state-
‘me nt that Potsdam quarries are found in Madison, Iron, and Reynolds
counties. ~The marble beds will be spoken of in the summary of the
Cambrian rocks of Missouri.”

* n a paper upon “The Geological History of the Ozark Uplift” Prof.
G. C. Broadhead describes, in 1889,° in a general way rocks referred to

iferons were deposited in Archean valleys of erosion, for they generally repose
nes arly horizontally, or with slight inclination, upon the Archean.*

EASTERN BORDER OR ADIRONDACK SUB-PROVINCE.

_ This includes the area about the Adirondack Mountains of New
York and the adjoining portions of Canada to the north. -
Ina report of the geological structure of the county of Saratoga,
M ir. J. H. Steele states that a conglomerated mass of rock is found in
the town of Greenfield not far from its south line, on the southeast side

He says:

It consists of rounded pebbles of quartz, from the size of a small shot to that of a
man’s head, united into one common mass by a kind of coarse ferruginous sand. It
extends along the mountains to no great distance, but fragments of it lay scattered
in all directions, and, indeed, are found along the whole extent of the south line of

t J town of Greenfield, and in various other places.®

_ Under the heading of “ Coarse Siliceous sandstone” a description is
yiven of an extended horizontal stratum along the west part of the
orth line of the town of poaloes Springs, and some way into the town
of of Greenfield: S34 7

+e atu
I Sis ‘@ coarse, hard rock, resembling common quartz in its fracture, but it is more

oose and granular in its structure. It is of a white color, and when heated and
tl 7 into water, crumbles into a fine white sand. * * * Ihave been somewhat
at \ loss to know where to place this formation, but from several circumstances I am
ident it should be placed among the oldest of the transition class.®

The ‘Southeastern Missouri lead district. Am. Inst. Mining, Eng., Trans., vol. 5, 1877, p. 102.

| arble | of southeast Missouri. Kansas City Review, vol. 5, 1882, pp. 524-526.

e Bik, Geolozict, vol. 3, 1889, Pp. . 6-18.

~~ 604 cit., p. 8.

roa “report of the geological structure of the county of Saratoga. Memoirs of the Board of Agricul-
rf ‘the State of New York, vol. 2, 1823, p. 53.

f the Kayadarosseras Mountains, resting upon the primitive rocks.

up he would prefer to assign all the rocks from the lower sandstone |

-

\

RN bie ete VR Ye pe a

> a. Se
eS q a bh ere Pm » 7.
0 oe \ - Ju eet \ Ae \ eg Fe Xo 8 Ee apie we Pee

> . re 4 ve aie -

202-0 >= se rin CAMBRIA, eee a

A dcannrption, is also given of a Caleareous sandstone as. it occ pe
on. the west side of the Kayadarosseras Mountains.! The sandstond
referred to by Mr. Steele, and also the lower portion of the Caleareous ii
sandstone, are now known to be of Upper Cambrian age. =” 2

Various references are made by Prof. Amos Eaton to the Calciferous ©
sandrock (or Transition sandrock) as examined by him in the valley of ©
the Mohawk. Healso says: “ Perhaps the Transition sandstone of the
Green Mountain series may not be connected with that of the Macomb |
Mountain series.”2. Most of Prof. Eaton’s references to this formation |
are very indefinite, and he included it with the Calciferous sandrock, as
exposed at Little Falls in the valley of the Mohawk. That he was
aware of its stratigraphic position is shown by the comparisons made
between the Transition sandstone of the Green Mountains and that of —
the Macomb Mountains, the latter now being known as the Adiron-
dacks.

The attention of Mr. J. H. Steele was ‘called to the oolitic formation’ :
about 2 miles from the village of Saratoga Springs. He described the
occurrence of great quantities of valcareous concretions of a most sin gular_ .
structure ; they are mostly hemispherical, but many of them are globular |
and vary in size from half an inch to that of 2 feet in diameter; they are
obviously composed of a series of successive layers, nearly parallel and
perfectly concentric, ete. This is the first notice of a fossil that was
subsequently described by Prof. James Hall as Cryptozoon proliferum. .
. It oceurs in layers in which the Upper Cambrian or Dikelocephalus-
fauna is found a few miles west of Saratoga Springs. a

In the first annual report of the geological survey of New York
Dr. Emmons mentions a sandstone resting on the primitive rocks both
on the Lake Champlain side of the Adirondack Mountains, at Whitehal ES
and on the western side, in the vicinity of Theresa, on the Indian River.®
In this preliminary paper the Calciferous sandrock of Prof. Eaton and vl
the subjacent sandstone are not clearly differentiated. In the secor
‘report, however, he separated the sandstone as the “ sandstone of Pots: 5
dam.”° His description of the rock is as follows: +n

I shall not enter upon its geological relations any further than to state that. in 7
Potsdam and other towns in which it appears it uniformly rests on the primary
strata; andin no part of the county is there any rock which interposes itself betwe mn
it and ‘the Primary, so that it appears here as the oldest representative of the transi-

tion series. The identification of this rock with the sandstones along the south 2) rn.
border of Lake Ontario will be a matter of some difficulty. It is geologically below

as

-_

1Op. cit., p. 56. Pea
~ 2A geological and agricultural survey of the district adjoining the Erie Canal, 1824, p. 78. “a
3A description of the oolitic formation lately discovered in the county of Saratoga and State of New v
York. Am. Jour. Sci., vol. 9, 1825, p. 17.
4Cryptozoon, n. g.,Cryptozoon proliferum, n. sp. Description of Pl. vi, 36th Ann. Rep. N. y. State
Mus. Nat, Hist., 1884. d
5 First annual report of the second geological district of New York. First annual report of ti
geological survey of New York. Albany, 1837, pp. 106, 107. .
Report of the geologist of the second geological district of New York. Second annual repor 4
the geological survey of New York. Albany, 1838, p. 214. a

. aa
ee
. > SS ere
/ on

2

,

-

+
im) they Fea ees F -
s , ee, -~ S 4 _

as ADIRONDACK SUB-PROVINCE. 903.
peas , s

ys Bbhds the relation of an inferior rock.! -
ay vi s rock is a true sandstone, of red, yellowish red, gray, and sess ath Pe
slo rs. It is made up of grains of sand and held together without acement. Inter-
xed with thé siliceous grains are finer particles of a yellowish feldspar, which do
Bet cenontiany change the character of the sandstone, but they show the probable
e from: which materials forming it were originally derived, viz, some of the vari-
sof granite. Uniike, however, most of the sandstones, it is destitute of scales of
mica. The coloring matter of the rock is evidently oxide of iron, but unequally
fused through it, giving it intensity or deepness of color in proportion to its quan-
: In some places it is almost wanting, which makes it, when pulverized, a good
ma aterial for glass. The grains and particles in its composition are generally angular,
4 at where it takes the character of a conglomerate, as it does in the inferior layers,
th hey are frequently rounded. The thicker strata exhibit an obscurely striped appear-
ance, owing to prevalence of certain colors in the different layers.?

In the description of the sandstone on the Lake Champlain side in
sex County it is said:

This I consider the same formation I have described under the name of the “ Pots-
dam sandstone.” Its position is evidently beneath the Transition limestone and Calci f
@) ‘ous sandrock. It is very deficient in organic relics, though not entirely destitute
0. ‘them. It is unnecessary to repeat what has already been said of this rock; it is
parely quartzose or siliceous in its composition and finely stratified. It dips to the
rtheast at Port Kent, at an angle varying from 5° to 10°. The places where it
occurs along Lake Champlain are indicated on the map of a part of this county, to
Lich I refer the reader. This rock at Keeseville has been rent in the most remark-
ab ble manner; several fissures, the principal one of which extends nearly a mile, and
‘th ade which the Au Sable flows, have been opened by some convulsion in nature to
he depth i in some places of 100 feet, and from 5 to 20 feet wide. Near the bottom of the
fis re at the High Bridge, as it is called, I discovered numerous specimens of a small
bi ivalve mollusea, a Lingula. I found also, on examination, that the same fossil oc-
eurred through an extent of seventy feet at least, and so far as I could discover it was
t foeronly fossil inclosed in the rock. It is extremely thin and delicate, yet the shell

a

= Beorrectly preserved, and is probably one of the oldest inhabitants of the globe, as

ie rock in which they occur is the oldest of the transition series.%
ee

In the second annual report of the paleontological department of the
New York survey Prof. T. A. Conrad tabulated the formations to show
the order of superposition and some characteristic fossils in the tran-
si ion strata. On the primary occurs No. 1, formed of variegated sand-
stones (Potsdam sandstone of Emmons), bad the olive sandstones and
sla es, characterized by Fucoides serra. These are classified under the
Cambrian system of Prof. Sedgwick.

The base of the Lower Silurian isa gray calcareous sandstone, char-

ized by Lingula acuminata: This part of his table is as follows :4

LOWER SILURIAN STRATA.

“op.et p. 214.
ap p. Cit., p. 215.
‘0 ‘ cit., p. 230.

ee a fae {+_- ae | dl 8 ee ee ee es
hy 28s: 7" Ss < ~~ yey ck f ee a

- J “a ¥ ae ae j ee a i aire 2 3 EPS eh at: a artis i ‘Ss eS
; - ; ~ ‘ = iA $ 5 ~@ i recta x ae Agee
: ae, caesar

co Oe . “pe CAMBRIAN. Ps eR a ee
. CAMBRIAN SYSTEM c(SHDOWICR). gel ES .
$ ie ‘Olive sandstone and slate......-...---2-2+02---eee seeeee Fucoides serra « (Broug)) _
: Variegated sandstone (Potsdam sandstone of Emmons). sata . -- Dictuolites radian aS

Vv ; A. description of the geographic distribution of. the Potsdam sandem
stone in Clinton County is given by Dr. Emmons in the third annual
report of the New York State survey. He also describes its strati-- 7
graphic character and appearance, and states that at Flat Rock the
sandstone is more or less a conglomerate and coarser than at Potsdam
_-or Keeseville.! | - aq
A description of the Potsdam sandstone as it occurs on the western
side of the Adirondacks, in Jefferson County, is given by Dr. Emmons |
in his fourth annual report, as follows:? — . a
Lying unconformably upon the primary is the Potsdam sandstone, It is tie
forenext in the series. Itis a firmer rock, more crystalline, and less porous thea
the same rock in St. Lawrence, and especially that belonging to Potsdani. ‘
The only fossil found in it was a small linguloid shell called Tingula
ovata?
The presence of the Potsdam sandstone in Lewis County is noted by
Mr. Lardner Vanuxem, who states that the sandstone appears in the
northeastern part of the county in low ridges, with all the characteristics”
given by Prof. Emmons, in whose district itis an extensive rock.t ae:
~The Potsdam sandstone as it occurs in Washington County, upon —
_ the eastern side of the mountains, is described by Dr. W. W. Mather as —

»
x

a hard, siliceous sandstone, white, red, gray, yellowish, and frequently striped. It

~ is well developed at,Whitehall, where it has a thickness of 150 to 200 feet. It extends —
up the valley of Wood Creek in @ southerly direction by Comstock’s Landing, Imile 4
east of Fort Ann, and so on farther south, diminishing in thickness and becoming
interlaminated with finer-grained strata of grits, slates,and shales. Some of the

my strata of this rock are covered with the most beautifully characterized ripple-marks, —
as perfect as if just formed on the sand a a sea beach, while the rock is of the most

by

indurated kind of sandstone. “2

The only fossils noticed were fucoidal impressions. a

~The geographic distribution of the Potsdam sandstone about the Adi- oh

-._ rondacks is shown on the map of 1844 that accompanies the final repor
of the State geologists of New York. On a geological map of the Mid
=. dle and Western States by Prof. James Hall* the main geographic dis-
tribution is indicated and a small area on the southern side of the’ Wis-

y consin River in Wisconsin is the same tint as the Potsdam area of Ne a
York. >

“1 Third annual report of the second geological district. - Third annual report of the geological su
vey of New York, 1839, pp. 231, 232. “a
_ #¥Fourth annual report ofthe survey ofthe stonii geclogical district of New York. Fourth aaa
- report of the geological survey of New York. Albany, 1840, p. 322. ae
> 3Qp. cit., p. 323. ig
4 4Fourth annual report of the geological survey of the 3d district. Fourth Report of the Coole gica “a
Survey of New York. Albany, 1840, pp. 363, 368.

™ =o 5 Fifth annual report on the geological survey of the 1st geological district. Fifth Axinual Report of re
the Geological Survey of New York, 1841, p. 102. >
Geological map of the Middle and Western States. Geol. of New York. isdn on the Fou at th
Geol. district, Albany, 1843. _ ‘ "ers an =,

5-8 me

1
s
7

: J - ar ae
¢ ; ‘ 4 ; 2 > on ae tired

yI che in 1842, Prof. T. A. Conrad states that the Cambrian sy bars
proved to be the Lower Silurian, and he places the Potsdam sand-
stone > ab ae base of the latter system, beneath the Calciferous sand-
sone. -

q othe final report of the geology of the second geological district con-.
t 8 asummary by Dr. Emmons of the characters of the Potsdam sand-
stone as found in the counties of Warren, Essex, Clinton, Franklin, St.
Tawrenee, and Jefferson, and also gives details of the formation as
und in each county.2” A description of the formation in detail and |
€ falso a general descriptive summary of the formation is given by Mr.
La ardner Vanuxem as it occurs in his district,* and Dr. W. W. Mather
¢ escribes it as it occurs in Washington County and in Saratoga County. —
Prof. James Hall describes it concisely in an account of the rocks of
New York State. In its geographic distribution the rock is known in
; Canada, on Lake Superior, and, from its position, it is probably the
Ba zine that appears on the Mississippi River mentioned by Dr. Owen in
the report on the lead region of the northwest.’ He also identifies it
“Ww vith No.1 of the Pennsylvania survey, or a sandstone extendin 1g threugh |
New J ersey, Pennsylvania, and Virginia.® :
In the account of his travels in North America Sir Charles Lyell de-
bac ribes the Potsdam sandstone as he saw it at Au Sable Chasm, near
JX ceeseville, Essex County, New York. He speaks of it as a siliceous
fs “sandstone:

: In many places, this most ancient of the fossiliferous rocks of New York (the Pots-
_ dam sandstone) is divided into laminz by. the remains of innumerable shells of the
genus Lingula. They are in such profusion as to form black seams like’ mica, for
. which they were at first mistaken. With the Lingula occurs another placunoid shell
allied to, if not identical, according to Prof. E. Forbes, with a fossil which occurs in
“0 pany with a small Lingula in the lowest beds of the English Silurian series at
<: ik in Brecknockshire.’

aN general account of the Potsdam sandstone is given by Dr. E. Em-
m nons in the Agriculture of New York. It is an excellent summary of
the general characters of the formation.®

. The Potsdam sandstone of Lewis County is described by Mr. F. B.

He ough in a general manner. He states that it thins out to an unim-
pe 01 eeer sare tum as compared with the formation in St. Lawrence County;

also that the superjacent Calciferous sandrock is represented by only a
: oy -

_ 1 0bservations on the Silurian and Devonian systems of the United States, with descriptions of new
‘+ ) ganic remains. Phila. Acad. Sci. Jour., vol. §, 1842, pp. 229, 230.

Geology of New York, part 2, second geological (northern) district, pp. 102-105, 177-179, ete.

pi Geology of New York, part 3, third geological (central) district, Albany 1842, pp. 28, 29.

. Eee Geology of New York; geology of the first (southeastern) district. Albany, 1843, p. 418.

. EGerbey of New York; geology of the fourth (western) geological district. Albany, 1843, p. 27

Op. cit. ; p- 28.

“Travels i in North America. New York, 1845, vol. 2, pp. 131, 132.

* Agriculture of New York, vol. 1, 1846, pp. 117, 118.

Sk

~

+
%

pe ee SESS ih? 20h © ir ae a as
ws: Me a ¥ £5 fe 2 Resa te) hee eer Be -
* > alts ae
> 5 ry. 7) abe ay er ex NPC =v
> * ;" — a . ~i* iy ah

206 | Se eS THE CAMBRIAN 3 3 won,

thin layer of the fucoidal Rania In 1850 he eatled: attention ig :
cylindrical masses from 8 inches to 15 and 20 feet in diameter that occur |
in the Potsdam sandstone near Somerville, St. Lawrence County? =
The description and accompanying figure recall the Cryptozoon proli-
ferum described by Prof. Hall from the Potsdam formation of Saratoga —
County. A year later attention was again called by Mr. Hough to the
cylindrical masses. They are described as vertical cylinders from 2-
inches to 20 feet and upward in diameter, and show a concentric struc.
ture. Numerous smaller bodies, not larger than an orange, of a sphe.
roidal structure are also met with in the vicinity. No traces of organic |
life were observed in the matrix. It is evident that these bodies are-
_ unlike the Saratoga Cryptozoon. aa
A more extended definition of the Potsdam sandstone was given by
Dr. E. Emmons in 1856. He then ineluded with it the lower sandstone
of the upper Mississippi Valley, and No. 1 of the Pennsylvania survey.* ty
An excellent summary of the existing knowledge of the Potsdam ;
sandstone was given by Dr. J. J. Bigsby in 1858 in a paper on the Pa.
leozoic Basin of the State of New York. A description is given of the
mineral characters, mode of transition, stratigraphic position, inode of
occurrence, thickness, and paleontologic character.® -
In a tabulation of the succession of sedimentary rocks Prof. Richarll
Owen states that the Potsdam sandstone of New York geologists is con- :
sidered by some English writers as belonging to a separate-sy Svein the S
Cambrian.® ;
The presence of the peculiar cylindrical masses in the Potsdam sani
stone mentioned by Mr. Hough is also noticed by Mr. T. G. B. Lloyd | in’
Jefferson County,’ but without any attempt to explain their origin ¢ or
nature.
In a note on the geology of Port Henry, New York, De T. S. Ho nt
states that the Potsdam sandstone and the basal member of the over-
lying Paleozoic series is well seen in a railway cut near Port Henry.
The lower beds are massive and compact, dark bluish or iron gray, with
lighter bands and thin, blackish, shaly layers. The only fossils observed
were Scolithus lindatid! and 8. panadentaes of the Potsdam of the Ota
Basin.’

1 Observations on the geology of Lewis County, New York. Am. Jour, Sci. and sche 2 vol. 5, 184
p- 273.
_ 2 Catalogue of mineralogical] and geological specimens received from F. B. Hough, 3d Annual Rep of
Regts. Univ. State Cab. Nat. Hist, 1850, pp. 32, 33.

3 On the cylindrical structure observed in Potsdam sandstone. Am, Assoc. Proe., vol. 4, 1851, pps
352-354. ~ ae i

4 American Geology, containing a full statement of the principles of the science, with full ilustra-
tions of the characteristic American fossils. Albany, 1856, vol.1, pt. 2, pp. 128-132. iM ag

5On the Paleozoic Basin of the State of New York. PartI. A synoptical view of the nineralogi Zice
and fossil characters of the Paleozoic strata of the State of New York. Quart. Jour. Geol. Soc., Lon -
don, vol. 14, 1858, pp. 338, 339. a

6 Preliminary observations; general report and description by counties. (Lower and Upper §
Tian). eS AS reconnaissance of Indiana, made in 1859-’60. one 1862, -p. 14... Sa

Pai

ey _ A short i. of the discovery of a massive limestone superjacent to
i the Q typical Potsdam sandstone containing species of the Potsdam fauna
€ equivalent to the fauna of the upper horizon of the lower sandstone of
the Mississippi Valley was made by Mr. ©. D. Walcott in 1884. The
ee was originally referred to the Calciferous formation.!

_ Mention is made of the contact between the Potsdam sandstone
fea the subjacent pre-Cambrian rocks in the vicinity of Fort Ann,
> Ww ashington County, New York, by Mr. ©. E. Hall.’

_ A section of the Potsdam sandstone with the superjacent limestone,
y crying the Upper Cambrian fauna was published by Mr. C. D. Wal-
- eott in 1886 accompanied by a list of the fossils found and a comparison
| set them with the Wisconsin fauna referred to the Potsdam by Prof.
ames Hall.’

In the fifth annual report of the State geologist of New York, in
‘some field notes on the geology of the Mohawk Valley, with a map,
Messrs. C. E. Beecher and C. E. Hall describe a section that occursina_
eut on the West Shore Railroad at “Little Nose, Randall, Montgomery
County, New York.”* Inthe woodcut illustrating the section, a breccia
that occurs unconformably beneath the Calciferous seater is stated
to contain Potsdam sandstone, crystalline limestone, quartzite, ete.
| The evidence upon which the fragments of sandstone were identified as
_ of Potsdam age is not given.

In a paper on a great Primordial quartzite Prof. N.-,. Winchell r re-

correlates the formation with the “granular quartz” of the western
# slope of the Green Mountains and the pre- ‘Cambrian quartzites of Wis-
eeonsin and Minnesota. ®

Ina paper read before the Geological Society of America, at Wash-
ington, ,D.C., December 31, 1890, Messrs. N.S. Shaler and H.8. Williams
de scribed the presence of a ea bed of shale beneath the Calciferous
-sandrock and just above a thin bed of sandstone that rests unconform-
ably upon the subjacent pre-Paleozoic rocks. The locality is a quarry
at Little Falls. In the shale numerous specimens of Lingulepis acumi-

. na ata were found.$

CANADIAN EXTENSION.

aie”
<=

In a report of progress of the geological survey of Canada for 184546
‘Sir r W. BE. Logan notes the presence of a sandstone in the Ottawa dis-

trict, but is doubtful whether it represents: the Potsdam sandstone, as
‘- ES De. ee ee!

pa Potsdam Anes at Saratoga, New York. Science, vol. 3, 1884, pp. 136, 137.
? Laurentian Magnetic iron ore deposits from northern New York, accompanied by a geological map
* f Essex County. Report of the State geologist for the year 1884. Albany, 1885, p. 32.
+ Second contribution to the studies of the Cambrian faunas of North America. U.S. Geol. Survey,
Bull. No. 30, 1886, pp. 21, 22.
Be “4Fifth Ann. Rept. State Geologist of N. Y., for 1885. Albany, 1886, p. 10. .
Bag erect Primordial Quartzite. Am. ae vol. 1, 1888, pp. 173-178.

oe

v
es

Epublistos a description of the Potsdam sandstone by Dr. Emmons and —

_

~ it may be i in the lower beds of the Caleifercug.t In a later report he

ing an exposed thickness of 45 feet and conformably subjacent to the

‘Potsdam sandstones in Canada was read by Dr. T. S. Hunt before the

_ conglomerate, with quartz pebbles, and it has some red layers; but towards the top
_ it becomes a fine-grained, hard, white sandstone, and at the summit it is interstrati-
fied with calcareous layers, forming a passage to the rock which overlies it.+

_ Murray describes the sandstone along the shores of the St. Lawrence

~ 1852-’53, 1854, p. 109. a

= = a Pe le HE fe ae SS = | wel a
Bt Be FT ST a iss etre ea
™ < el Fin apie ys he 5 ta
; eS Se eed ee Sw SER aS <s
bs 4 £ ; a ger Ge 4K é
208 © Rt eee THE ‘CAMBRIAN. | es gts me Poe on

- on . a < = . +e ay

noted the presence of the Potsdam sandstone on the north shore of the
St. Lawrence at Murray’s Bay, 90 miles below Montreal, describing it q
as a formation consisting of white, translucent, slaty quartz-rock hav-

Calciferous sandrock.? a
A brief summary of the lithologie and paleontologic characters of the

American Association for the Advancement of Sciencein 1851.3 =

In an extended paper on the foot-prints occurring in the Potsdam.
sandstone of Canada, Sir W.-E. Logan describes the Potsdam sandstone
as it occurs in Canada in the St. Lawrence Valley. He states that— _

- The sandstone in Beauharnois County and the neighboring part of the State of 3
New York is from 300 to 700 feet thick. In the lower part it contains many beds of

The description of the extention of the Potsdam sandstone between
the River of the North and Beauharnois was continued by Sir W. EH.

Logan in the report for 1851~52.5 In the same volume Dr. Alexander

in the vicinity of Brockville, and also in the Olea exposed between L
the rivers Ottawa and St. Lawrence.® =

This was followed in 1854 by the account of Dr. Murray's exploration n
between Kingston and Lake Simcoe. In this region the Potsdam is
not largely developed, the greatest thickness of it observed in any onal
place being certainly not over 40 or 50 feet, while west of Knowlton
Lake, in Loughborough, it appears gradually to decreanes in thicknes S)
and eventually to die out altogether.’

In the summary of.the work of the Geological Survey of Canada from
its commencement to 1863, there is given a very complete description
of the stratigraphic, lithologic, and paleontologie characters of the Pot ‘
dam sandstone as known in Canada.’ Since that time ERY little has
been published upon the formation.

1 Report on sequence and distribution of the formations (on the Ottawa). Geol. Surv. Can ini,
Report of progress for 1845-46, Montreal, 1847, p. 51. 4

?Report on Bay St. Paul and Murray Bay. Geol. Surv. Canada: Rébics of progress for. 1848 “49
Toronto, 1850, pp. 10, 11. oom

3 Remarks on the lithological and paleontological characters of the Potsdam sandstone. Am. ‘Asso 0G.
Proc., vol. 6, 1852, pp. 271-273.

4Qn the foot-prints accurring in the Potsdam sandstone of Canada. Quart. Jour. Geol. Soc., Lon
vol. 8, 1852, p. 200.

* Report [on country bebinca Riviére du Nord and Beauharnois] Geol. Surv. Canada, 1851-’52. 185
pp. 8-14, - ‘
® Report-[of country lying between rivers Ottawa and St. Lawrence] Geol, Survey of Canada £
1851-52, 1852, pp. 64-67. a

7 [Exploration between Kingston and Lake sappiis Geol. Surv. Canada: Report of progress f

a

8 Geological Survey of Canada: Report of progress from its commencement to 1863. Menizoal 18
pp. 87-109.

-

Be * cues BORDER OR ROCKY MOUNTAIN SUBPROVINCE. -

=, : COLORADO.

he ¢ probable presence of the equivalent of the Potsdam sandstone
f the Mississippi Valley in the Colorado range was noticed by Dr. F.
V V. Hayden i in 1874. He says:

The lowest beds of sedimentary rocks are rather coarse sandstones, and conglom-
e rat e made up of water-worn quartz pebbles, with very irregular lamin of deposi-
, the whole reminding one of the Potsdam group. * * * There is considerable
ra wee in the aggregate of beds here, which may be regarded as Silurian, and we may
200 clude that the Potsdam group is quite well represented, and that it is possible

ion
iar

in dy, yet it is an interesting fact to know of their existence in this locality. In
e lower sandstones I found a species of Lingula, the present season, probably a
sdam form.!

bove Colorado Springs. Of the probable presence of the “ Potsdam”
bbe South Park, on the north slope of Mount Lincoln, and on all of
she eereanding high mountains he does not appear to have any doubt.
€ says: ;

B fore going farther I will state what I believe to be the age of all the lime-
t ‘0 nes and quartzites which seem to cover the highest mountains, and in which
mo st of the valuable mines are found. I think there is no doubt that they belong
v1 he Potsdam group, though I was unable to discover any fossils. Dr. Peale found
v y obscure forms which indicated that the group is of the same age as those next
oth ie granites in Utah, which we now know are of that age.?

|. ©. Peale examined and measured a number of sections passing from
various horizons in the superjacent rocks to the Archean. In one, ex-
* ing from Glen Eyrie eastward to Camp Creek, there are 40 feet of
ise sandstone of a grayish white, dark green, gray and brick red
a or. This series rests upon the granite; is beneath limestones re-
‘red to the Quebec group, and is considered to represent the Potsdam
$ roup.? od

On Trout Creek, in enon Park, 93 feet of sandstone is referred to
1¢ F Potsdam.! Ina reddish sandstone superjacent to the ** Potsdam”
nt umber of fossils were found that were referred to the Quebec group.
on 2n0w known this fauna is of Lower Silurian (Ordovician) age, cor-
Z a onding to the Calciferous zone of the New York section. Another
Be ti on was measured on one of the eastern tributaries of Trout Creek,

Besoin rt of F. V. Hayden, U.S. Geologist. U.S. Geol. Surv. of the Terr., 7th Ann. Rep., 1874, p. 35.
Op. cit., p. 41.

ort of A.C. Peale, M. D., geologist of the South Park Division. U.S. Geol. Surv. of the Terr.,
n. Rep., 1874, p. 202. _
Op cit., p. 208.

& _ Bull. 8i——14

MAB ome ze We Se Pa eee ER RR Se SQ PRES LS
i, SP Sip 3S RM is ce i i eae a ie eat Sears
+. 3 a : A ie ewer FY OS a ¥ P 4
Meise ~~“ “COLORADO. 323 209
+ oan ; ‘ ;
Ei a 4
ta, 7

at some of the higher divisions occur. These rocks require a still more careful

; These observations were made eu William’s Cafion, 2 or 3 miles —

While studying the geology from Denver to Colorado Springs, Dr.

oe - >> (~*~ - = bs hi Pr > Ved ae are Peo tos a bt

| Sg te Bs ORNS ome

f dat 5 Pe Pee uaF,

YS | | tate . ‘THE ‘CAMBRIAN. Eo ie ean ee fu Be

in which 67 feet of sandstone ocsur resting upon the saginats or these
sections Dr. Peale says: . ‘ a
A comparison of the sections given above shows-that the Potsdam gtoup is eal |
sented by sandstones having a thickness of from 60 to 80 feet, while the beds that
represent the Quebec group are a little over 100 feet thick.!
References to the sandstone supposed to be Potsdam are also found
on pages 226, 236, 242, and 255.
During the field season of 1874 Dr. A.C. Peale found on Eagle Rive

‘a series of beds resting on the gneiss and schist. From their positio D
and lithologic relations to corresponding beds seen in the Colorado
Range in 1873 the lower layers are referred to the Potsdam group. It
is represented by a bed of white quartzite.”
A reference to the probable occurrence of the Potsdam horizon upon 1
the eastern side of the Colorado Range is made by Mr. Arnold Hague,
in his geueral description of the geology of the range. From the fact r
that a sandstone occurs in the Black Hills, and contains fossils of |
Primordial type, he thinks the sandstone occupying a similar atratil
graphic position in the Colorado Range will be found to contain the
same fauna. 4 -4
On the geological map of Colorado, published by Dr. Hayden i in 1877,
the quartzite and the limestone referred to the Potsdam series are in-
cluded with the Silurian, and their geographic distribution is merged
with the latter on the map. ‘J
In his synopsis of the geological formations found in Colorado Dr. F
M. Endlich tabulates the localities and formation of the « Potsdar
group. 4 =
When describing the Paleozoic rocks of the Mosquito Range i in ce en
tral Colorado, Mr. 8. F. Emmons states that the Cambrian is represent
by quartzites passing gradually upward into calcareous shales, wit
limestones of probably Silurian age above, the aggregate thickness c
the two being about 400 feet.’ In the tabulation of the Mosquito see
tion the Cambrian white quartzite is given a thickness of from 150 t
200 feet before passing into calcareous and argillaceous shales aboy e
The only fossil remains found in this series occur in a bed of greenis
chloritic slates on the east flank of Quandary Peak, about a mile ana OV
the Monte Cristo mine. They belong to the genus Dikelocephalus ai
resemble closely Dikelocephalus minnesotensis of the Potsdam form
tion. From analogy with other sections Mr. Emmons thinks it anf
assume that the fossiliferous shales occur above the main body |
quartzite and near the base of the transition series.’

~

1 Op. cit., p. 209. >

2 Report on Middle Division. (Stratigraphy-Paleozoic formations). U. S. Geol. and Geog. =——
the Terr., Ann. Rep. for 1874, 1876, pp. 110, 1il. ~
SBiras, Arnold, and §.F,Emmons. Descriptive geology U.S. Geol. Expl. of the Fortieth —
Clarence King, vol. 2, 1877, p. 29. aa
4Report of F. M. Endlich, geologist of the White River Division. U.S. Geol. Surv. of the Ter
10th Ann. Rep., 1878, p. 130. a
5Geology and mining industry of Leadville, Colorado. Mon. U.S. Geol. Survey, wal, 12, 1886, pd
6 Op. cit., p. 57. 7 Op. cit., 2 60. is EST

Ce hes e. na +

_ : Sy

——— oe

Err he eye ee REE IE, TN EN
Eee. i Ss! Pi. bs cay > Oe ic
‘ee Te ee) -. Ae, ees Pt i yee le " ; 3
pacere ys Se A WYOMING. | 211.
WYOMING.

As eolbp lat to Capt. Reynold’s expedition to the headwaters of the
Eitissoari and Yellowstone Rivers, Dr. F. V. Hayden identified, in 1861,
the fossiliferous “‘ Potsdam ” sandstone of the Black Hills, and ae
_ ered a sandstone holding the same relative position and exhibiting the
4 same lithologic characters on the slopes of the Big Horn Range as the
Same formation. It is further stated that ‘a few thin layers of fine
_ calcareous sandstone were observed filled with fossils characteristic of
this period.”! |

qi From the Big Horn Range he preaed to the Laramie Range. At the
head of the La Bonté Creek he noticed a bed resting discordantly upon
= zoic slates 50 to 100 feet in thickness, holding the same position and
a eens the same lithologie characters it reveals at other localities.
I could discover no fossils in it at this point, but I am confident that this bed rep-
4 esents the Potsdam sandstone. This rock (the Potsdam) is more or less changed by
heat from beneath, but I was able to trace it continuously from the source of the
m Chu gwater Creek to the source of Cache la Poudre, a distance of over 100 miles, It
was also seen along the eastern slope of the Wind River Mountains, but ae not con-
‘ fain any organic remains.?

RAL more extended account of the character of the Primordial aud
stone of the Rocky Mountains was published by Dr. Hayden in 1862.3
‘Iti is accompanied by a description of the species of fossils found in the
E ack Hills and the Big Horn Mountains and further reference to it
will be found in the account of the Cambrian rocks of Wyoming.

_ All of the essential part of Dr. Hayden’s article of 1861 was reprinted
* an article on the Geology and Natural History of the Upper Mis-
enti, which appeared in 1863.4 This essay is, as stated by the author,
t the substance of a geological report made by him to Capt. Raynolds on
the exploration of the Yellowstone and Missouri Rivers. The latter
I report was issued in 1869, accompanied by a large map, dated 1859~60,
at ps on which the etait distribution of the formations identified ri
I . Hayden are delineated. Within the present area of Wyoming a
a 1row belt of the ** Potsdam ” sandstone is represented as entirely sur-
. per unding the Big Horn Mountains, and as forming a continuous band
‘ith that along the eastern side of the Wind River Range and an in-
ferrupted belt on the western side of the latter range. The two moun-
— now known as the Wyoming Mountains also had a narrow band
pf G Potsdam ” sandstone aboutthem. ‘To the north this band is repre-
e: sented as continuing westward across the Big Horn River, then north
on 1 the western side of the Yellowstone Lake region as far north as Bea-
ver Bee? where it is interrupted. Several mountains directly north

—) S kétch of the geology of the country about the headwaters of the Missouri and Yellowstone Rivers
é Am. . Jour. Sci., 2d ser., vol. 31, 1861, p. 234.

-2 ‘Op. cit., p. 234.

_ 8The Primordial Sandstone of the Rocky Mountains in the Northwestern Territories of the United
*s. -Am. Jour. Sci. 2d ser., vol. 33, 1862, pp. 68-79. Canadian Jour., new ser., vol. 7, 1862, pp. 149-151.
n the Geology and Natural History of the Upper Missouri. Am. Philos. Soc. Trans., vol. 12, new

-

—

SMR RW gS gt Se as Se ees ae ae ae et
: ; tee Sh ss ie a pay ae har Oe Ses
Se heed to 2 PR 1 ees ee
to : : “t a
es ae . Rene eee
“2ITZ ; ; “THE CAMERIAN, SRS RS
— ‘ ys aT hae « i -

these limestones ‘they are immediately underlaid by about 300 feet of

4th Ann. Rep., 1871, p. 33.

_ §PDescriptive geology, U. S. Geol. Expl.of the Fortieth Pér.; Ciarence King vol. 2, p. 76. Washih ng

of the Yallowsions Lake region are rihjnesbabeld as surrounded by the ;
same formation. :

At the South Pass of the Wind Rivér Mountains Dr. Heades ‘toast’
the granites occupying a very restricted area and extending from them |
a large thickness of ‘‘ Potsdam” sandstone containing Qbvlella nana
and a Lingula.?

Prof. F. H. Bradley in 1873 identified the ‘ Quebec group” ‘by. thal 3
presence of Conocoryphe and Dikelocephalus in limestones upon the
flanks of the Teton range of mountains. At one of the outcrops of —

partly compact, partly shaly, glauconitic sandstones, which are evi-—
dently equivalent to the so-called Knox sandstones of Safford, which |
form in Tennessee, the lower part of the Quebec group. No fossils
were seen in tlcse beds. They are apparently unequally distributed, —
since no corresponding beds appear along the cafion of West Teton —
Creek. Beneath them, and often present when they are absent, we
generally find from 50 to 75 feet of a very compact ferruginous quartz
ite which must represent the Potsdam, though this also, is sometimes
wanting.”*? In a diagram of a section extending from Henry’s Fork
through the Teton Mountains the so-called Quebec group and Potsdam
quartzite are represented on each side of the range, the quartzite et F
ing directly on the granite.* i

The preliminary paleontological report of Mr. F. B. Meek refers the ie
beds containing fragments of Conocoryphe and Dikclocepkalus, foun a
on the west base of Big Horn Mountains by the Hayden survey in 1872,
to the Potsdam or Primordial zone. ®

In speaking of the Paleozoic rocks of the ieararate Hills, Mr. Avagh a
Hague states that all paleontologic evidence obtained from these beds S
would tend to show that they belong to the Coal Measufe limestone.® ¥ 4

The strata along the eastern slope of the Wind River Mountains re-
ferred to the Potsdam by Dr.Hayden were studied by Prof. T. B. Co n-
stock while geologist of Capt. W. A. Jones’s expedition to northweste an
Wyoming. He found the sandstone closely resembled that described
by Prof. J. D. Whitney in Wisconsin. The local peculiarities of th is
sandstone and its associated rocks as described in the Mississippi Val-
ley and New York are strikingly repeated in the Rocky Mountain
region. The greatest thickness of the sandstone in the region of @

1 Gevlogical report of the Exploration of the Yellowstone and Missouri Rivers. Under the direct
of Capt. W. F. Raynolds, 1859-’60, Washington, 1869, p. 144, map. re
2 Report of F. V. Hayden (on the geological survey of Wyoming.) U.S. Geol. Surv. of the ts rr.

3 Report of Frank H. Bradley, gcologist of the Snake River division. U. Geol. Surv. of the’
6th Ann. Rep., 1873, p. 216. , aes

4 Op. cif., p. 218. : |

5Preliminary paleontologicalreport . . . with remarks on the ages of the rocks, etc. U. Ss. Geol
Survey of the Territories, embracing portions of Montana, Idaho, Wyoming,and Utah ; 66th Ann. | =
1873, p. 431. Re

ton, 1877. 7 ea

_—

d r 4 y a
. : % ‘ ; ~ : & + a

BEER RR on are Sot eee
ee eet Ne re ee
eee ees: 3 x

a j. - Z os WYOMING. 33 213

osbaiealgy in ‘shallow seas or upon hosted or sand flats. !
é Under the head of Quebec group, Prof. Comstock describes some
a ploiferons layers and dolomitic limestones that are conformably super-
acent to the sandstone. In them he found a species of Theca?, a tri-
Jobite of the genus Dikelocephalus and Orthis tritonia? Fragments of
other fossils too imperfectly preserved for identification were found.?

ay If the identifications by Prof. Comstock of the species found in the
r imestone are correct, that portion of the limestone containing them
must be referred to the Upper Cambrian zone. On the map accom-

en itire eastern margin of the Wind River Mountains and along the west-
arn central portion of the range. A narrow belt of it surrounds Creek
Mountain in the northeast of the Snake Indian Reservation, and the
Ww yoming Mountains to the northwest of the Wind River Range.
poke southern portion of the Sweetwater district in the Wind River
Range was visited by Dr. F. M. Endlich in 1877. He found a Lingula,
p robably Lingula prima, and estimated the thickness of the entire series
as varying between 180 and 320 feet. He refers to the Calciferous
“group a thin series of sharply bedded strata composed of blue lime-
stones and blue and yellow dolomite and locally of oolitic dolomite,
altogether having a thickness of about 250 feet.t These strata are cor-
‘related with those containing Dikelocephalus, etc., discovered by Prof.
Comstock i in 1874,
; 4 The Teton Mountain district was studied by Prof. Orestes St. John
‘ir a 1877, and in his report he refers to the work of Prof. Bradley in 1872.
Ve very little is added to the information given by Prof. Bradley of the
lower quartzite series, but an important advance is made in the classifi-
ation of the rocks of the district by the division of Prof. Bradley’s
Qi iebec group into the Upper and Lower Quebec limestone. The Lower
Quebec limestone, carrying Conocoryphe and Dikelocephalus, is de-
scribed in detail and separated from the upper limestone carrying
Ra taphistoma, ete.’
_ The line of separation of these two limestones is the line between the
Cz mbrian and Silurian (Ordovician) Systems, and reference will be made
to it under the description of the Cambrian rocks of Wyoming.
% Prof. St. John also studied the Buffalo Fork Mountain, east of the
ton Range, and found there the same succession of beds as in the
" Be ton section. Numerous fossils were collected from the limestone over-
¢ the quartzite.®
76 Geological report. Report upon the reconnaissance of northwestern Wyoming, made in the sum-

mel r of 1873, by William A. Jones. 1874, pp. 107, 108.

3 zor. cit., p. 110.
pepert on the geology of the Sweetwater district. U.S. Geol. Surv. of the Terr., 11th Ann. Reps,

——

ee 4 ,p- 72.

® Report of the geological field-work of the Teton Division. U.S. Geol. Surv. of the Terr,, 11th Ann,
Rep., 1879, pp. 481-483,

Or cit. p. 469.

a

as

ae ee te ss ee ee » "= oe hee ee SO
— y ~~” : ‘ :

45 pe anying the report the ‘‘ Potsdam” formation is represented along the .

~~ eastern sides of the Wind River Range, that he refers to the Silarian.?

214 zn Sep CAMBRIAN, (Pa ee emer

In his report on the cedlaeg of the Wind River ilintrict, made in 1883, 4
Prof. St. John describes the geology of the Gros Ventre Range, accom- a
panying it with two plates of sections across the range at various. |
points.!. On the map accompanying the volume the geographic distri--
bution of the strata referred to the Silurian is delineated. He also
describes the out-crops of the strata on the northwestern and north-

Reference to Prof. St. John’s sections will be made in describing the
Cambrian rocks of the Wind River and Gros Ventre Ranges.

On the map accompanying the twelfth annual report of the Hayden 4
survey, issued in 1833, the geographic distribution of the strata referred
to the Silurian in the Sweetwater Range, the Wind River Range, the
Gros Ventre Range, and the Teton Range is shown. The Silurian in-
cludes the quartzite referred to the Potsdam, the Cambrian limestone |
referred to the Lower Quebec by Prof. St. John, and the Calciferous
referred by him to the Upper Quebec. This map was compiled from the
work of Messrs. Peale, St. John, and Endlich. There is also a special
map showing the district reported on by Prof. St. John in 1883.

>
DAKOTA,

The presence of evenly bedded sandstones about the Black Hills was
noted as early as 1822 by Dr. Edwin James, who represented them
upon a diagrammatic section, extending from the Alleghany to the
Rocky Mountains. He undoubtedly confused the sandstones of the
Trias with those of the Cambrian ; but it is one of the earliest recorde od
illustrations of the mode of paeaweenbe of the sandstone in this region.
That he did not penetrate to the interior portion of the hills is evident,
as his section represents the sandstone extending in level horizon al
layers entirely across the area occupied by them.’

In 1856 Mr. H. Engelmann published a description of. the rocks of the
Black Hills. The strata next to the granitic nucleus are described a
“more or less altered sandstones and limestones, dipping in varie
directions and degrees. Most of the sandstones are fine grained, light™
yellowish red, and do look much like metamorphic, but some show tla |
transition into a siliceous rock.”* Not far from camp 56 he found <
friable sandstone made up of coarse square grains of granite, appar-
ently deposited after the formation of the igneous rocks. Near can] p
58 the sandstone is light yellowish red and fine grained. There is also
a gray variety, above which is a layer of a dark red sandstone, coarse
grained, soft, and highly micaceous.' This is the sandstone in which
Dr. Hayden subsequently found the Upper Cambrian fauna. ;

1 Report on the geology of the Wind River district. U.S. Geol. Surv. of the Terr., 12th Anno
Report, 1883, p. 208. Aa
2Op. cit., pp. 251-253. il
3 Geological sketches of the Mississippi Valley. Phil. Acad. Sci., Jour., vol. 2, pt. 2, 1829, pp. 326- -
4 Report of a geological exploration from Fort Leavenworth to Bryan’s Pass, made in connection w th
the survey for a road from Fort Riley to Bridger’ 8 Pass, under Bryan. Rept. ss of War, Appendix H
1856, p. 508. ca
_ § Op. cit., p. 510. 9 y

‘
e es a
i. 4

“. DAKOTA, ~ 915

bra ska al ae in 1858 Dr. F. V. Hay dent states ‘that the existence
of th he Potsdam sandstone on the eastern slope of the Rocky Mountains
was discovered during Lieut. G. K. Warren’s expedition to the Black
H ills i in the summer of 1857.

In March, 1858, Messrs. Meek and Hayden presented a paper to the
Academy of Natural Sciences, Philadelphia, containing ‘‘ some remarks
| on the geology of the Black Hills and portions of the surrounding coun-
try.” In this a section of the formations is given, in which the “ Pots-

A

tain Lingula, Obolus ?, and fragments of trilobites.2, The sandstone is
described as of a sidioh and grayish color, composed of angular grains
C of ‘quartz, cemented by siliceous and sometimes small portions of calea-
re reousmatter. Thefossils then identified were Lingula antiqua Hall, great
n numbers of a small shell similar to LZ. prima Conrad and fragments of

- Hayden was also published in the American Journal of Science,* the
Canadian Naturalist (vol, 3, 1858, pp. 182-193), the report of the Chief
of Engineers to the Spbrctary of War, 1858,° the American Journal of
Science (vol. 25, 2d ser., p. 439, 1858), the Proceedings of Philadelphia
A Academy of Science (vol. 10, p. 139, 1859), and in a reprint of the Pre.
ti minary Report of the aadonsilinn of Nebraska and Dakota, issued in

ti ransmitted to the Chief of Engineers.

In a paper on the Primordial sandstone of the Rocky 1] Mounkatns and
Northwestern Territories of the United States Dr. Hayden describes
ee sandstone he referred to the Potsdam in the Black Hills in eon-
siderable detail, as follows :6

f 3. Variegated sandstone, of gray and ferruginous red color, composed chiefly
ae of grains of quartz and particles of mica, cemented with calcareous matter,

Beck friable grit, others aconglomerate. Fossils: Lingula prima, L. antiqua, Obo-

a _ A. Stratified azoic rocks standing in a vertical position for the most part.
_.The “Potsdam” sandstone is again described by Dr. Hayden in
1863, 7and in the following year he published, in connection with Mr.

&

7

oP Explorations under the War Department; explanations of a second edition of a geological map of
Nebraska and Kansas, based upon information obtained in an expedition to the Black Hills under
command of Lieut. G. K. Warren. Am. Jour. Sci., 2d ser., vol. 26, 1858, pp. 276-278.

: _*[Some remarks on the geology of the Black Hills and portions of the surrounding country.] Phil
Acad. Sci., Proc., vol. 10, 1859, p. 44.

» 20p. ot ae 49.

_ 4£xplorations under the War Department; explanations of a second edition of a geological map of
N Yebraska and Kansas, based upon information obtained in an expedition to the Black Hills under
& mmand of Lint. G. K. Warren, Top. Engr., U.S.A. Am. Jour. Sci., 2d ser., vol. 26, 1858, p. 276.

“4 5 Catalogue of the collections in geology ana natural history Sitalaven by the expedition under com-
cm nd of Lieut.G. K. Warren. Appendix to Rept. Sec. of War in Rept. of Topog. Eng, for 1858. (Re-
' print edition of 1875, pp. 59-125. Map.)
= 6The Primordial sandstone of the Rocky Mountains in the Northwestern Territories of the United
‘States. Am. Jour. Sci., 2d ser., vol. 43, 1862, p. 70.

F a On the geology and natural history of the Upper Missouri. Am. Phil. Soc. Trans., vol. 12, new

ser. nets, p. 36-38.

a d

= =<

dam” sandstone is given a thickness of 30 to 50 feet and is said to con- |

rilobites.? Theinformation contained in this first paper by Messrs. Meek

1875, which is the official account of Lieut. G. K. Warren’s exploration

a? - Some portions of the bed are very hard, compact, siliceous; others a coarse’

lella nana, and fragments of a trilobite, Arionellus? oweni. . . 50 to 80 f.

a Meek, the Pe ars of the fossils he found in the Black Hills dusheel ’

172, 1864, pp. 2-10.

& *

216 Bae orae THE CAMBRIAN. ge Se

the aipedition of 1858. They.are Lingulepis pinnaformis, D. see ’
Obolella nana, and Agraulos sp. aq
_ A general description of the sandstone of the Black Hills is given by a
Prof. N. H. Winchell in his report to Capt. William Ludlow, and the
geographic distribution of the outcrop in the southern portion of the
Black Hills is shown on the accompanying map? In the same report —
Prof. RK. P. Whitfield® describes Obolus pectenoides, a new species of |
brachiopod, and also figures Lingulepis pinnaformis.
The report of Mr. Henry Newton on the geology of the Black Hills
contains a detailed description and full discussion of the strata referred —
to the Potsdam sandstone. This will be again referred to in the sum:
mary of our knowledge of the Cambrian rocks of the Black Hills.* From ‘
the paleontologic portion of the report we learn that the entire fauna .
of the Black Hills below the Carboniferous is Primordial, and Prof. Re
P. Whitfield states it closely resembles that from Wihebianiie and al-
though the species are nearly all distinct the generic facies is the seinen
throughout.® ,
In 1888 Prof. F. R. Carpenter published a series of notes on the geol-
ogy of the Black Hills, in which he criticised some of Newton’s views, —
and also advanced some theoretical considerations of interest in rela- 4
tion to the original deposition of the sediments forming the Potsdam

- group.® : “

SOUTHWESTERN SUBPROVIN CE,

This includes the areas of Texas and Arizona.

TEXAS. a. 4

The presence of Silurian rocks in Texas, subsequently referred to the
Primordial, was announced by Dr. F. Roemer in 1849.7 In the same —
work he describes from the lower portion of the section Lingula acutan- .
gula (p. 420) and Pterocephalia sancti-sabe (p. 421). 4

On the map accompanying this volume the entire Paleozoic series is
included under one color, on the northern side of the granitic. band,
northwest of Austin. a

Sm la hice ee rr
1 Paleontology of the Upper Missouri; a report upon collectious made principally by the expedition —
under command of Lieut.G. K. Warren in 1855-56. Invertebrates. Smithscnian Contributions Nog

2 Geologicai report of a reconnaissance of the Black Hllis of Dakota, made in the summer of 1874 by
Captain William Ludlow. Report of the Chief of Engineers, Appendix PP, 1876, p. 1170. ;,
3 Description of new fossils. Report of Geological Reconnaissance of Black Hills. Appendix PP o: B
Report of Chief of Engineers, 1876, pp. 1202, 1203.
4Geology. Section IV. The Silurian. The Potsdam sandstone. U.S. Geog. and Geel. Surv. of the E
Rocky Mountain region, J.W. Powell in charge; report on the Black —_ of Dakota. —_ Pp.
80-107. .
5 Paleontology of the Black Hills of Dakota. Report on the geology and resources of the Black i
of Dakota. 1880, pp. 329, 330. - 4
6 Notes on the geology of -the Black Hills. Preliminary Rept. Dakota School Mines on Ee? Bi:
Hills of Dakota, 1888, pp. 11-52.
7Texas. Mit besonderer Riicksicht anf deutsche Auswanderung und die physichen Verhaltn
des Landes nach eigener Beobachtung geschildert. Boxn, 1849. een, aS.

ee Bo ots Bey hs Rs, pa =< eS -. oh iA, 4 ; ig - ~-h.
BA eg te et RL :
RE se ae. ty oat
Le Saar A ae ee TEXAS. 217
nia arte > - ret
“ive East * -~

A ‘more extended account of the geology and the paleontology was
) publisl hed by him in 1852, in which he notes the occurrence of Silarian
ro ks in Llano County, on the San Saba River (p. 7); and describes
and illustrates Lingula acutangula (p. 90), Pterocephalia sancti sabe (p.
‘ 2), and the genus Pterocephalia. Attention is called by notes and
eures to two undescribed species of trilobites.:
i a letter addressed to the Secretary of the St. Louis Academy of
viences in 1859 Dr. B. F. Shumard states that he had discovered in
Bu rnet County, Texas, an extensive development of Lower Silurian
‘roc ks, equivalent to the Potsdam sandstone and the Calciferous sand-
rock of the New York system. The Potsdam sandstone is filled with
trilobites belonging to the old genus Arionellus, with Obolus and Lin-
S ula, and a small Orthis, and it rests directly upon the granite. Above
the e Potsdam we have beds which appear to represent the third mag-
-nesian limestome and second magnesian limestone of the Missouri sur-

‘the Primordial zone of Texas, accompanied by a number of sections
cored i in Burnet County, and a description of new species of fossils
fr from limestones referred to the Primordial. Under the heading of ‘‘Pots-
a Jam sandstone” three sections are given;‘one, 5 miles northwest of
; eee town of Burnet, has a thickness of 275 feet. In this fossils were
bundant in the upper portion, just beneath the Cretaceous limestone,
s well as in the lower beds. The base was not seen. This section is
a de up almost entirely of limestones, as are the other two sections
- mentioned.*

_ Dr. Shumard states that the Potsdam sandstone is also finely dis-

gins of the granite districts of Llano. ‘The fauna of this division of
t ne Primordial zone of Texas is very analogous to that of the Potsdam
" sandstone of Iowa, Wisconsin, and Minnesota.” The genera identified
are : “ Dikelocephalus, Bathyncad: Arionellus, Conocephalites, Agnos-
tus, Lingula, Discina, Orthis, Camerella, Obolus, and Capulus, all of
W which genera have been discovered in the Primordial sandstones of the
orth west except Agnostus and Camerella.”* In the latter part of the
aper Six new species were described, and a species of Camarella and
ne of Capulus mentioned. Ina ioe to M. Barrande, dated Septem-
de sr, 1860, Dr. Shumard describes in a general way the Primordial rocks
of Texas as seen along the Colorado River in Burnet County.°
_ Attention was called in 1874 to the presence of a sandstone in Organ
‘Mountains, close to the city of El Paso, in southwestern Texas, by Mr.

pe
Ry

ch
0

B
s

“1Die Kreidebildungen yon Texas und ihre organischen Einschlusse. Bonn, 1852, pp. 92, 93.

Spee touching the late discovery of Lower Silurian rocks, equivalent to the Potsdam sandstone

i Calciferous sandrock of the New York system, in Burnet County, Texas. Trans. Acad. Sci. St.

I ouis, vol 1, 1859, pp. 672, 673.

Ps *The Primordial zone of aerate with descriptions of new fossils. Am. Jour. Sci., 2d ser., vol, 32,
a » PP. 216, 217. 2

“Op. ¢ cit., pp. 217, 212.

% ‘Letter on the Primordial of Texas. Soc. g6ol. France, Bull., 2° sér., vol. 18, 1861, pp. 218, 219.

i.

i
a
Se

te Two years later_Dr. Shumard published a more detailed account

i played in the southern part of San Saba County and around the mar-

eee <, i uae — : PN OE 8 eg Ak >. Re DE a Re the ee ee oe a. ee
be TS ak ad ee Pi Sag fe Met oe ee Big tape NS hy OT,
ik ey a eae Me y 3 SSR NS TS OL Rae PO ee ¢
: = 2 . ' : > yey “rn > bs > 7 ~ 7 wy ae oe ie s ys
é a, ~ = 5 oe eo a > a —s ‘ *»
V5; Seo | THE CAMBRIAN. —~ Prete A ee Bl.
- . , ' ' ee

W.P. Jenney. He lates that the quartzite rests $ tipon a coarse felds-
pathic granite, and passes upward into sandstone, filled with Scolithus
linearis, which he identified as the Potsdam sandstone. The superjacent —
formation is a crystalline limestone identified as calciferous. It con- |
tains several species of fossils resembling Archeocyathus, and rarely a —
gasteropod, like Pleurotomaria.! In commenting upon the statements ;
of Mr. Jenney, Prof. J. S. Newberry says: |

Now it appears there are found in the Rio Grande Valley the crystalline base. _
rocks overlaid in succession by the Potsdam and Primordial, the Trenton, Hudson, —
Upper Silurian (?), and Carboniferous, just as they occur in the Northern and Eastern —
States. * * * It would seem as though the Organ Mountains had formed one —
- border, and the New York and Canadian highlands the other, of the great Paleozoic
invasions of the sea.?

A section of the strata referred in 1874 to the Potsdam by Mr. 8S. Ba
Buckley, at Packsaddle Mountain, in Llano County, gave athickness of |
385 feet of alternating limestone and sandstone, beneath which occurs —
a massive bed of reddish brown sandstone 326 feet in thickness. Numer- -
ous genera of Primordial fossils were found, characteristic of this hori- ,
zon.’ Other references are made tothe occurrence of the Potsdam —
sandstone at various localities in this county. In the report for the
following year Mr. Buckley refers to the occurrence of sandstones of
the Potsdam period in Mason and Menard Counties. He also calls —
attention to the probable presence of rocks of Silurian age at the base :
- .of the Organ Mountains at Fort Bliss, near the town of El Paso.* a

A preliminary report of a reconnaissance of a portion of the Paleo-
zoic area of central Texas was made by Mr. C. D. Walcott in 1884. A
measured section of the strata referred to the Cambrian on the west
side of Honey Creek Valley gives 245 feet of sandstone and 625 feet of -
limestone, all marked by the presence of an abundant Upper Cambrian —
(Potsdam) fauna. The upper beds of the limestone become compact, —
hard, and have a little included cherty matter. The Cambrian fauna —
terminates here, as far as observed, and it is not until over 1,000 feet of —
limestone are passed through that recognized fossils again occur. The :
fauna is then of the type of the Calciferous group.® The text is accom-— |
panied by a diagrammatic section of Packsaddle Mountain, that illus: | :
trates the unconformity between the Llano group and the strata re.
ferred to the Potsdam or Upper Cambrian. This gave a total thick-
“ness of 605 feet for the formation, with a massive sandstone 205 feet 1 it fr
thickness at the base.® ¢

The latest addition to our knowledge of the Cambrian rocks of Texas —

LO RE I a eS

1 [Recent explorations in the Geology of Texas.] New York Lyceum Nat. Hist. Proc., vol. 2, 1874,
p. 69.

2Remarks on geology of Western Texas. New York Lyceum Nat. Hist.. Proc. vol. 2, 1874, p. 70.

8¥First annual report of the geological and agricultural survey of Texas. Houston, 1874, p. 73. ;

4Second annual report of the geological and agricultural survey of Texas. Houston, 1876,p.10.

5 Notes on Paleozoic rocks of Central Texas. Am. Jour. Sci.,3d ser., vol. 28, 1884, p. 433. 7 ‘a

6 Op. cit., p. 432. : San

| Prof. 1. B. Comstock.) He divides the rocks referred to the Cam-
( V iddle Beaticias , and the Katemey (Potsdam) series (Upper Cam-

bri rian are represented i is based upon the presence of certain beds beneath
4 the fossiliferous Upper Cambrian. He considers that the Hickory beds
he we altogether a thickness of 200 to 250 feet. The maximum thick-
n ess of the Riley series is probably 300 to 400 feet. The upper or Kat-
| emey series is divided into, Division A, or the Potsdam sandstone,

thickness 90 to 140 feet; Division B, the Prisdom flags, probable thick-
on Bees 50 feet; Division 6, the Potsdam limestone, 200 fon. ;

2 as ARIZONA.

As geologist of Lieut. J. C. Ives’s expedition -to the Colorado River
of f the West, Prof. J. S. Newberry was the first one to recognize the
presence of a sandstone resting upon the Archean granite in the “ Big
—Caiion” of the Colorado. A diagrammatic cross-section of the eafion
Pepresenta the “Potsdam” sandstone unconformably superjacent to

— the granite and conformably subjacent to strata doubtfully identified

£ is largely developed in the Great Caiion is a coarse siliceous rock that
_ must have been derived from the erosion of land at no great distance.”
A section at Diamond Creek, as described by the same author, in-

which occurs 820 feet of sandstone. Of the upper beds of the sand-
stone, No. 10 of the section, Prof. Newberry says:

The foliated sandstones of No. 10 have an indescribable look of antiquity. They

_ are usually fine grained and hard, the lighter ones drab or gray, speckled with dark

= red. The shales above and below these sandstones are very soft red or green mud-
stones, containing great numbers of cylindrical bodies, which resemble the casts of

3 worm holes.

Nos. 12 and 13 are coarse siliceous rocks, having the same appearance of extreme

q age as No. 10, but much coarser and more massive. The lithological characters of

5 i res I have examined of that rock on Lake Superior and in Canada. * * * In
of these sandstones must be in some degree conjectural and liable to modification by
- the discovery of new facts; yet the evidence is in a good degree satisfactory that
they are the equivalent of the Potsdam sandstone of the New York geologists. The
indications of this identity are found in their great relative antiquity and in their
lithological characters.*

; 4 ‘Attention i is called to the resemblance of these sandstones to those

an

Z of the Black Hills which occupy the same relative stratigraphic posi-

¥ Surv, of Texas for 1889, 1890, pp. 285-289.
a Geological report. Report upon the Colorado River of the West, expl. in 1857-58 by Lieut. J. C.
_ Tves. Part 111, 1861, p. 42. ‘
-80Qp. cit., p. 47. ;
“ tonite 56.

_ these strata are strikingly like those of much of the Potsdam sandstone of the expo-

_ the absence of fossils, whatever conclusions may be arrived at in regard to the age

Bee ARIZONA. 218";

a n?). The supposition that the Lower Cambrian and Middle Cam-

as Silurian.” In the text it is said “the Potsdam (?) sandstone which —

D. eludes a conglomerate 3 feet in giiaiiocs resting on the granite, above |

tg 1A preliminary report on the geology of the central mineral region of Texas. 1st Ann. Rep. Geol. d

=

-

~

RIES ES SEUSS TES a Need ae ee
nd <2 be : PE eee at = , Sine: SP onetes wa Be Sn ~~
. / 3 a E ee Et aye . . ol 7 we ee ra o7
: $ : ‘ “ ay > ‘ ah % Pr Ae , r 4 ig et > ers le 4 ir mo
3 : ew ag: mg Whgsl 4 ¥ ee “So Se
22055" HSS oS rE CAMBRIAN. S ELS as :

~ This extends from the edge of the plateau down 3,500 feet, and beneath a

r<

tion, and iedaeds contain ‘ae Potsdam fauna, as identified by Dart

Hayden.! - pth

When describing the section of the Grand Cation of the Colorado: %

where it passes through the Kaibab plateau, Maj. J. W. Powell states. 4

“that the summit of the section was formed by Carboniferous limestone. E

it occurs 1,000 feet of conformable rocks of saudaterbnenl age. These
in turn piiead down to the unconformity between them and the subja-
_ cent 10,000 feet of strata that were subsequently referred to the Grand —

- Cafion group. At the close of the same paragraph, in speaking of the :

latter series of rocks, he says: .

The beds themselves are not conformable to the overlying Carboniferous rocks; ;
that is, the Carboniferous rocks are spread over their upturned edges.?

It thus appears that all of the strata down to the unconformity were © .

referred to the Carboniferous. This includes the series of sandstones —
referred to the Potsdam by Dr. Newberry.

As the result of his studies of the lower strata of the Colorado Cafion
region at Diamond Creek and at the mouth of the caiion, Mr. G. K. Gil-
bert in 1874 designated the series of sandstones referred to the Potsdam
by Newberry, as the Tonto group, and considered it to belong to the

Primordial division of the Silurian.? The data for this mip were —

published in the following year.*

The section at the mouth of the Colorado has 80 feet of vitreous 4

sandstone resting unconformably upon the granite, and 605 feet of

shales alternating with limestones between the sandstone and a super- q
jacent massive limestone.’ At the mouth of the Kanab Creek 100 feet

of green arenaceous and micaceous shales occur between the superja-
cent massive gray limestone and the level of the river.6 From the ©
stratigraphic position of the Tonto sandstone and shales and the pres-
ence of a species of the genus Cruziana he was led to conclude that the ©

Tonto group is certainly Lower Silurian in age, and probably Primor- “i

~ dial.”
The section of the Tonto series at the mouth of the Grand Caiion was
measured more in detail by Mr. A. R. Marvine in the same year. He

~ traced * the formation to the south and southeast along the margin of re

) Op. Cit., p. 57.

2Exploration of the Colorado River of the West and its tributaries, explored in 1869, 1870, 1871, and
1872. Washington, 1875, p. 212.

3On the age of the Tonto sandstone. (Abstract.) Washington Phil. Soc. Bull., vol. 1, 1874, p. 109.

4 Report on the geology of portions of Nevada, Utah, California, and Arizona examined in the years

1871 and 1872. Report on Geog.and Geol. Expl.and Survey west of the 100th merid.,in charge of -

Lieut. Geo-M. Wheeler, vol. 3, Geology, 1875, pp. 184-186. Report on the geology of portions of New
Mexico and Arizona, examined in 1873. Ibid., vol. 3, 1875, pp. 521, 522.
5 Report on the geology of portions of Novadh Utah, California, and Arizona examined in the years:
1871 and 1872. Report on Geog. and Geol. Expl. and Survey west of the lv0th merid., in charge of

Lieut. Geo. M. Wheeler, vol. 3, Geology, 1875, p. 163.

_ SOp. cit., p. 162. ; ae
7Op. cit., pp. 185, 186. -
8 Report on the geology of route from St.George, Utah, to Gila River, Arizona, examined in 1871,

-Rept. on Geog. and Geol. Expl. and Surv. west of 100th merid., in charge of Lieut. Geo. M. bel vie 4

vol. 3, pane: 1875, p. 199. ‘ ‘>.

«

%

_ Se ies. gaa ue pat ge he
oS a aaa aes tee yeh eae me
ee , re e * PALEONTOLOGY—UPPER_ MISSISSIPPI. OFT

the prelate a that extends southward from the Grand Cation. ‘The geo-
ap ohic lgiatetb ition of the formation is indicated on the atlas sheets -

blished by the Wheeler survey in 1874. .

~ When describing the sedimentary groups of the Plateau province

4 Maj. Powell accepted the name Tonto group, proposed by Mr. Gilbert,

bu t did not agree with him in considering the strata to be of Silurian

age. From geological considerations he was inclined to consider the
Tonto group as forming the base of the Carboniferous series. This
@ opi nion was strengthened by the fact that he found in the Grand Cajion
¢ ” feet of sandstone, shales, and limestones underlying the Tonto
eries. unconformably, and hence separated from them by long periods
: D f erosion, and at the base of the spupen series he reported finding Silu-
rian fossils.!
b- The fossils mentioned by Maj. Powell were studied by Dr. C. A.
Ww hite, who identified the genera Lingulella and Obolella and referred
them to the Lower Silurian.” |
_ The supposed Primordial age of the Tonto series was accepted by
» apt. C. A. Dutton in his account of the physical geology of the Grand
-Caiion district.
The section at the mouth of the Kanab Cafion was studied by Mr. ©. :
F D. Walcott in 1880. He found that 450 feet of a mottled limestone and
100 feet of arenaceous and micaceous shales at the base of the section
| _ were of Primordial age, as indicated by the presence of the genera Lin-
sg gulepis, Conocephalites, and Bathyurus in the upper portion, and in ad-
dition to these Hyolithes primordialis, Lingulepis, and Crepicephalus in
ihe lower beds. Further evidence of the Cambrian age of the Tonto
Be group was published by Mr. Walcott in 1883. Fossils representing the
‘ "genera Cruziana, Lingulepis, Iphidea, Conocephalites, Crepicephalus,
a nd Dikelocephalus were found in the upper 700 feet; of the sandstones,
4 = shales, and limestones that form the upper part of the group in the
eafion valleys entering on the left side of the Kaibab plateau.>

PALEONTOLOGY.

Fs.

UPPER MISSISSIPPI AREA.

a The first reference that we find to the fossils of the Cambrian fauna
_of the Upper Mississippi Valley is by Dr. D. D. Owen in his report of
1848 on a geological reconnaissance of the Chippewa land district of

‘As = ———

_. Report on the geology of the eastern portion of the Uinta Mountains and a region of conntry adja_

cent thereto. Washington, 1876, p. 56.

: _ *Invertebrate paleontology of the Plateau province, together with notice of a few species from —

ema beyond its limits in Colorado. Rept. on the geology of the eastern portion of the Uinta

r ‘ountains, by J. W. Powell, Washington, 1876, p. 79.

2 Bs 2 The physical geology of the Grand Cation district. U.S. Geol. Surv., 2d Ann. Rep. 1880-’81. 1882,
p14.

4 The Permian and other Paleozoic groups of the Kanab Valley, Arizona. Am. Jour.Sci., 3d ser., vol. 20, 7

, P. 225.

~ #Prevarboniferous strata in the ia es Caiion of the Colorado, Arizona. Am. Jour. Sci., 3d ser., vol.

a, p, 439

ae: aioe ee SCS IEE CERTAIN, ° 50S funn st

Wisconsin.' The fossils discovered were Rte to thie: genera Asa.
phus, Agnostus, Trinucleus, and Triarthrus, but on PIG accompanying —
the report, there is figured, but not named, the head saa pygidium on
Dikelocephalus minnesotensis, and a species of Ptychoparia as now
known. . .
In a later paper in 1851 on the paleontology of the lowest sandstones ~
of the Northwest he gives the uname “ Dikello-Cephalon” to a large
genus of trilobites obtained in the lower sandstone formation.?, He also
notes the discovery of Lingulas and Orbiculas by himself in 1847 at the —
Falls of St. Croix, and the discovery of fossils on the Mississippi River |
between the Falls of St. Anthony and the Wisconsin River, the pres- |
ence of trilobites in the sandstone 10 miles below Mountain Island, ete. —
One of the first species described from the *‘ Potsdam” sandstone of —
Wisconsin is Graptolithus hallianus Prout, 1851, from the middle por. a
tion of the formation at Osceola Mills, near the falls of St. Croix
River.’ =
The occurrence of the Potsdam fauna in the sandstone of northeast:
ern Wisconsin is noted by Prof. James Hall in his report to Messrs, —
Foster and Whitney.* He describes and illustrates Lingula prima Con- —
rad (p. 204), Lingula antiqua Hall (p. 204), and an undetermined species -
of Dikelocephalus (p. 205).
We note that Lingula prima was eae described by Hall as
Obolella polita, and that Lingula antiqua equals Lingulepis acuminata
of Conrad and the Lingulepis pinnaformis of Owen. — =
From the material collected from the lower sandstones of Wisconsin
(the Potsdam sandstone of New York) Dr. Owen Cones in 1852, the 4
following genera and species: ® 2

Dikelocephalus (n. gen.), p.573. | Lonchocephalus (n. gen.), p. 575.

minnesotensis, p. 574, chippewaensis, p. 576.
pepinensis, p. 574. hamulus, p. 576. z :
miniscaensis, p. 574, Crepicephalus (n. gen.), p. 576. 7
iowensis, p. 575. Menocephalus (n. gen.), p. 577. ; +e

granulosus, p. 575.

In the description of Pl. 1 the species Menocephalus minnesotensis is”
named and figured (Fig. 11); also Crepicephalus ? wisconsensis (Fig.
13), and on Pl. la, Crepicephalus (2) miniscaensis is named and illus- |
trated (Fig.14). On Pl.1b, the species Lingula pinnaformis is proposed -
and illustrated (Figs. 4, 6, 8); Linguia ampla is figured and named r

' Report of a geological reconnaissance of the Chippewa land district of Wisconsin; and incident. ©
ally, of a part of lowa and of the Minnesota Territory. Letter of the Secretary of the Treasure 'y com-
mnnicating a report of a geological reconnaissance of the Chippewa land district of Wisconsin (ete), 2
by D.D.Owen. Thirtieth Congress, Ist Sess., Senate Ex. Doc. No. 57, 1848, pp. 13-15. a
- 2 Am. Assoc. Proc., vol. 5, 1851, p.171. . ae

3 Description of a new Graptolite found in the Lower Silurian rocks near the falls of the St. Croix

River. Am. Jour. Sci., 2d ser., vol. 11, 1851, p. 189. ae, P

4 Description of new or rare species of fossils from the Paleozoic series. Rept. on the geology of the
Lake Superior land district, by Foster and Whitney, pt. 2, 1851, pp. 203-231. 3

5Geol. Surv. of Wisc., Iowa, and Minn., and, incidentally; of a portion of Nebraska Territory. Phila
delphia, ly . ,

-

Pigs 5, 12), sigethver with eee of f Lingula antiqua and L. prima, and
a number of others placed under Obolus and Orbicula.

rs. .> _ Mr. Edward Daniels stated in 1859 that upon a small island in Black
~ River he had found perfect impressions of crustaceans consisting of
; double rows of parallel tracks, precisely like those in Montreal.! (Pro-
— tichnites of Logan.—C. D. W.)

j . In the report of the superintendent of the geological ITS, of Wis-
_ consin, Prof. Hall describes, from the Potsdam sandstone: ’

= Lingula polita, p. 24. Theca primordialis, p. 48.

Lingula aurora, p. 24. _ Serpulites murchisonia, p. 48. A

In the geological volume he illustrates : °

*
°

a
od

Pery

ag Graptolithus(Dendrograptus)hal- Theca primordialis, p. 21.
—- lianus, p. 21. Serpulites murchisonii, p. 21.
oe ‘Lingula polita, p. 21. Dikelocephalus minnesotensis, p,
gall pinnaformis, p. 21. 22,
. ES 2 antiqua, p. 21. D. pepinensis, p. 22. .
aurora, p. 21.

Tn a letter to Principal J. W. Dawson, Prof. Hall describes a new
- erustacean from the Potsdam sandstone under the generic name of
pe biacnts, stating it to be the same form mentioned ina communication
a the Albany Institute.‘

In 1862 Prof. C. H. Hitchcock published a list of the fossils of the
- Potsdam group in North America, including in it all the species known
_to him described from the Potsdam sandstone and also from the strata
¥ now referred to the Cambrian of other parts of North America. The
~ list includes one hundred and thirty-four species.

293

: F. In 1862 Prof. B. F. Shumard describes from the Potsdam sandstone —

of Wisconsin and Missouri the following species :°

eo a Dikelocephalus latifrons, p. 101.
| Arionellus bipunctatus, p. 101.
Conocephalites minor, p. 105.

He also noticed under the name of Conocephalites towensis, the Ditkel-

& ~ ocephalus (2) iowensis of Owen (p. 102), and Crepicephalus (2) wisconsensis, —

under the name of Conocephalites wisconsensis (p. 103). The Loncho-
3 _ cephalus chippewaensis Owen and L. hamulus. are both referred to the
- genus Conocephalites (p. 104). A species of Agnostus was referred to
: BA gricine orion (?) of Billings (p. 105).

a

«

4 _ 1 Notes on 1 geology of Wisconsin and adjacent States. Boston Soc. Nat. Hist. Proc.,; vol. 6, 1859, p.
—-310..

9 __ ?Report of the superintendent of the geological survey (of Wisconsin), exhibiting the progress of

_ the work, January 1, 1861. Madison, 1861, pp. 52.

r *Physical geography and general geology. Geol. Surv. Wisconsin, Report, vol. 1, 1862, pp. 1-72.

_ 40n anew crustacean from the Potsdam sandstone. Canadian Naturalist, vol. 7, 1862, p. 445.

_ ° §Fogsils of the Potsdam group in North America. Portland Soc. Nat. Hist. Proc., vol. 1, 1862, pp.

+) 87-90. >

_ * Notice of some new and imperfectly known fossils from the Primordial zone (Potsdam sandstone

a and Calciferous Sand- -group of Wisconsin and eo St. Louis Acad. Sci. Trans., vol. 2, 1862, pp. —

101-105. ;

Se SOE RRR eo near nes a en
5 4 “=, 4 - a

e = o gis See : q ye m a = : he
= : wa wre 7 . o> at ae Cb Sat = e
~ > " - : : z r om Pes SA Aas NE oa €y
?* *. a.“ Pw tT hm a ae ¥ SS ers
224 % THE CAMBRIAN. ae EP ¢ aos e
- a +. £ _ . Q a.

In the same year Prof. James Hall read béeore' the Pere Institute -
a preliminary notice of the fauna of the Potsdam sandstone, with re:
marks upon the previously known species and descriptions of somenew
ones from the sandstone of the Upper Mississippi Valley. - This was first
published in the Sixteenth Report of the State Cabinet of Natural His-
tory in 1863, and in 1867 in the Transactions of the Albany Institute.
The new genera and species described are as follows:!

Lingula winona, p. 126. . eryon, p. 157. :
mosia, p. 126. anatinus, p. 158.
aurora var., p. 127. patersoni, p. 159,
Discina(?) inutilis, p. 130. ? binodosus, p. 160. oa
Orthis pepina, p. 134. -winona, p. 161. vs
Platyceras primordialis, p. 136. diadematus, p. 167.
Euomphalus (?) vaticinus, p, 136. Ptychaspis sp.?, p. 174. :
Dikelocephalus miunesotensis . Chariocephalus whitfieldi, p. 175.
var. limbatus, p. l41, Illenurus quadratus, p. 176.
Dikelocephalus minnesotensis Triarthrella auroralis, p.177.
var., p. 141. . Agnostus josepha, p. 178.
Dikelocephalus spininger, p. 143. . parilis, p. 179.
misa, p. 144. disparilis, p. 179.
osceola, p. 146. . Aglaspis barrandi, p. 181.
Conocephalites eos, p. 151. Pemphigaspis bullata, p. 221.
perseus, p. 153. Amphion? matutina, p. 222.
shumardi, p. 154, Conocephalites ? (Arionellus ta
nasutus, p. 155. dorsalis, p. 222. 3g
oweni, p. 155. Conocephalites optatus, p. 222.0 “
Of species previously described he redescribed and illustrated:
Graptolithus hallianus, Prout., as Dendrograptus hallianus, p. 124, ; —

‘Lingula ampla, Owen, p. 125.
aurora, Hall, p. 126. >
pinnaformis, Owen, as Lingulepis pinnaformis, p. 129. ‘4
Obolus apollinus Owen, as Obolella? polita, p, 133. cane Be
Lingula? polita Hall, as Obolella? polita, p. 133, oS
Theca primordialis Hall, p. 135.*
Serpulites murchison}, Hall, p. 136.* *

~ Dikelocephalus minnesotensis, Owen, p. 138. ; ae
pepinensis, Owen, p. 142. : ax -
Conocephalites minor, Shumard, p. 149. <u re =f
minutus, Bradley, p. 150. a

Dikelocephalus iowensis, Owen, as Conocephalites iowensis, p. 162. =e

Crepicephalus? wisconsensis, Owen, as Conocephalites winconsensis, p. “164,

Lonchocephalus hamulus, Owen, as Conocephalites hamulus, p. 166, eer

Arionellus bipunctatus, Shumard, p. 169.

Dikelocephalus miniscaensis, Owen, as Ptychaspis miniscaensis, p. 171.
granulosus, Owen, as Ptychaspis granulosa, p. 173.

_ Agnostus orion (?) Billings, noted by Shumard, is described as Agnos- 4
tus josepha (p. 178). The genus Dikelocephalus is redefined (p. 137),

! Preliminary notice of the fauna of the Potsdam sandstone, with remarks on the previously known a
species of fossils‘ and descriptions of some new ones from the sandstone of the Upper Mississippi —
Valley. 16th Ann. Rep. Regents Univ. State Cab. Nat, Hist., 1863, pp. 119-2 20. Albany Inst. Trans. see a
vol. 5. 1867, pp. 93-195.

2 Pages 135, 136 each have an asterisk (*) placed after them to indicate interpolated pages. Le ee - : aye.

! SS
- \ ie 5 OY ie
xe >
“

feeans ‘Obolelta o of Billings i is ‘asesisbadlt with areolal reference
ecies Obolella polita (pp. cies | ; :
The new genera described are:

-— Lingolepis p. 129.

‘cers. p. 170.

ree ariocephalus, p- 175.

-‘Iilenurns, p. 176.

_ Triarthrelia (subgenus), p. 177.

°. S Aglaspis, p. 181.

s Pemphizaspis, p. 221.

he genus Conaspis is proposed i in the event of a new generic group
eing formed of Conocephalites perseus, C. shumardi, C. nasutus, C.
i eo 0. eryon, ©. anatinus, and C. patersoni (p. 152).

Prof. Hall states that he was unable to recognize the six successive
ilol ite beds of the sandstone as indicated by Dr. Owen, but he
eX Rctheless refers the species described to three different epochs of

he Potsdam period, as follows:

In the lower beds of the formation I have: found Conocephalites proper, together
1 Lingula, Lingulepis, Obolella? and Theca. In the middle stage, neither the
il sof the beds, nor the range of species or genera, have been so well determined ;
B, grouping together all that I have found between the well-defined upper beds
nd d the lower fossilferous beds known, we have Conocephalites, Dikelocephalus, Ari-
vellt us, Ptychaspis, Chariocephalus, Winmarad and Agnostus, in the trilobitic fauna,
ether with Orthis and Platyceras.
he >» Graptolitide apparently begin their existence somewhere in this central epoch,
it their precise relations to the other beds have not been determined.
In 1 the higher beds of the formation, and clearly separated from the great central
ne oe have the genera Dikelocephalus, Triarthrella, and Aglaspis, together with
Jingula, Serpulites, and Euomphalus.
Weo observe, therefore, that the earliest trilobites are referable to the genus Cono-
ephe ites; and the genus Dikelocephalus does not appear in the first stages of the
rmation, nor below the beds which I have referred to the second or middle stage of
eriod. There this genus appears in three species, smaller and less conspicuous
1086 i in the higher beds. It is only in the later stages of the sandstone that
he ® typical species of this genusof Dr. Owen appear, and those from the lower beds, :
n us F re ferred by him, belong apparently to other genera,!

= ‘rom a small collection of fossils from the Potsdam sandstone of
ik County, Wisconsin, Dr. Alexander Winchell deseribes in 1864
new. species and mentions the presence of some others that have
eer deceived 2 The new species are :

9g Orthis barabuensis, p. 228.

ae _ Straparollus (Ophileta) primordialis, p. 298,

_ Pleurotomaria ? advena, p. 228.
--Piychaspis barabuensis, p. 230.

va Superior sandstone he describes Paleophycus Wetichlaltee (p.
m i P. informis (p. pals The two latter species are doubtfully re-

of | a small collection of foasils from the Potsdam Sandstone of Wisconsin and Lake Superior
ne of Michigan. Am. Jour. Sci., 2d act, vol, 37, 1864, pp. 226-232.

Bull. 81—15 > é 3

Ja
wt at

ee

. ferred t to the Oumbsan fan In this papene Dr. Winchell points. out t,
-. or, rather, ‘he claims, that Dikelocephalus and. Ptychaspis ‘oceur at
| the recognized base of the Potsdam sandstone.) ek

by Prof. J. Hall, was published with illustrations in 1863, as has been

the Albany Institute. The descriptions are the same as those of the )

species : 3 | Pe ape
-Paleophycus plumosus, p. 50. Ptychaspis striatus, p. 55s
Triplesia primordialis, p. 51. minuta, p. 55.
Palzxacmea irvingi, p. 51. Agraulos (Bathyurus ?) woosteri,
Bellerophon antiquatus, p. 52. Oe ~

Conocephalites calymenoides, p. Arionellus (Agraulos) convexus,
52. p. 57.

_Crepicephalus onustus, p. 53. Ellipsocephalus curta, p. 58.

description of the species. These tracks or trails are congeneric w ith
- Climactichnites wilsoni, described by Logan in 1863, from Perth, Canada.

5, barabuensis, Winchell, as Leptzna barabuensis, p. 171.

' sin. Geol. Surv. of Wisconsin, Ann. Rep. for 1877, 1878, pp. 50-58. e

vol. 5, 1882, pp. 276-281.

se teed SM Oe stl NE Naa ke Tae CSS 9 OMB OTT oN Yo tas
I am, z - 3 oy < oR ere px <TD * a5 ef Baac: ae Re Dae a ies Se rapper a seg
, - ~ > - >} *¥
Oo 1 ave FY Pe? a OD “eh
DIRS ce eee THE -CAMBRIAN, ok. So
eae sk li ak 2 a
> - 3 4 a <a =# eon aig Sheet *”

- *

The preliminary notice of the fauna of the eatadain aanristaa: “off
the upper Mississippi Valley read before the Albany Institute i in 1862,

noticed. The original paper appeared in 1867 in the transactions of

paper of 1863, with the exception of the omission of those of Theca |
primordialis ana. Serpulites murchisoni. |

From the material collected by the Wisconsin Geological Survey Prof. a
R. P. Whitfield described in 1878 under the title of Potsdam sandstone

Dikelocephalus granulosus, Owen, is redefined under Ptychaspis gram
losa, but not the Ptychaspis granulosa of Hall (p. 54). Ptychaspis granu-
losa, Hall, is redescribed as P. striata (p. 55). %

In 1879 Prof, T. C. Chamberlin referred to some tracks found on ‘the
Potsdam sandstone by Rev. A. A. Young, of New Lisbon, Wisconsin.
He named Climactichnites youngi and C. fostert. The material was sub-
sequently studied by Mr. J. E. Todd, who published an illustration and

4a

In 1882 in his final report on. the paieoitelogy of Wisconsin, Prof
R. P. Whitfield described from the Potsdam sandstone the following
new species:* | -

Holopea sweeti, p. 174. Dikelocephalus lodensis, p, 188.
Conocephalites ? quadratus, p. Aglaspis eatoni, p, 192. :
180. Arenicolites woodi, p. 177.
Onrees ?) ay Aap p. ,
181.

He also describes and cliente ;

Paleophycus plumosus Whitf., p. 169.
Lingulepis pinnaformis, Owen, p. 169.
Orthis pepina, Hall, p. 170.

Triplesia primordialis Whitt., p. 172.

1 Op. cit., p. 226. d
2 Preliminary descriptions of new species of fossils from the lower geological Pa a of Wisco

3 A description of some fossil tracks from the Potsdam sandstone. Wisconsin Acad. Sci., 13 ‘TanS4

4 Paleontology (of Wisconsin). peoPer. of Wisconsin, vol. 4, 1882, PP. 169-193. : Le, ee ae

> : : ? roy ao er
= : It a we ee
- nade Se) at a e+e
~ ™ e £ ~ ie -
4 hp hee eae wie

PAC sa irvingi, p. 173, + ) :

ihe coperlloe (Ophileta) primordialis, Winchell, as ; Ophileta (Raphi-*
es stoma) primordialis, p. 173. 3

Bt Th eca primordialis, Hall, as Hyolithes primordialis, p. 175.

Bellerophon antiquatus, Whitf., p. 176.

Co nocephalites calymenoides, Whitf., p. 179.

a BF Crépieephalus onustus, Whitf., p. 182,

FS ee ereebiealitos gibbsi, Whitf., as Crepicephalus? gibbsi, p. 184.

_ Dikelocephalus granulosus, Owen, as Ptychaspis granulosa, p. 185.

_~ Ptychaspis granulosa, Hall, as P. striata, p. 186.

a minuta, Whitf., p. 186.

_ Dikelocephalus minnesotensis Owen, p. 187.

a - Agraulos (Bathyurus?) woosteri, Whitf., p. 189.

- Arionellus (Agraulos) convexus, Whitf., as Arionellus convexus,
Whitt., p. 190. ISS

f _ Ellipsocephalus curtus, Whitf., p. 191. 2

In n the preliminary remarks on the fauna he says:

-

We
P

patie of considerable interest that, in different localities of the Potsdam es:
ion, the forms of trilobites found are generally specifically distinct; and not- ~
anding the large number of species already described from this Loita liete both
State and other parts of the country, other new forms, readily detsatad by
familiar with the several details of structure peculiar to these animals, are met
th at almost every new locality examined. This change in species between dif- -
r rent localities i is usually accompanied also b y some slight difference in the material
q position of the rock, which not only shows that the species were of short dura-
( 1 time, or that they were restricted to limited geographical areas, but that a
s in the conditions of life and circumstances under which the animals existed,
id with which they had to contend, was constantly taking place. How much these
reumstances or conditions had to do with the production of forms, or modification
E tyr xs among them, it would be difficult to determine; but one thing is certain, —
ab where the same character of rock and apparent conditioas of deposition prevail
ra limited geographical area, or are repeated within a slight vertical range, we _
etty sure to find the same, or closely allied forms represented, showing that

<

like conditions similar forms prevail! _ he

: In 1883, when describing the life of the Ponditinas epoch, in the Gen- ;

al Geology of Siena Prof. T. ©. Chamberlin illustrates the fol-
vin ng species :* }
- Palwophycus plumosus, p. 125, Fig. 11.
; * _ Bellerophon antiquatus, Whitfield, p. 126, Fig. 12, sat
ie _Ophileta primordialis, Winchell, p. 126, Fig. 12, ¢, d.
_ Holopea sweeti, Whitfield, p. 126, Fig. 12, e
% aa - Palwacmea irvingi, Whitfield, p. 126, Fig. 12, i
_ Platyceras primordialis, Hall, p. 126, Fig. 12, g.
_ Serpulites murchisoni, Hall, p. 126, Fig. 12, h.
o x Theca primordialis, Hall, p. 126, Fig. 12, i.
_ Dendrograptus hallianus, Prout, p. 126, Fig. 12,j.
¥ Lingula antiqua, Conrad, p. 127, Fig. 13, b.
E cs -‘ Lingulella stoneana, Whitfield, p. 127, Fig. 13, a.
as 1 aurora, Hall, p. 127, Fig. 13, c.
_ampla, Hall, p. 127, Fig. 13, d.
mosia, Hall, p. 127, Fig. 13, e.

t., pp- 163. 164, :
era Bescelons:, “Historical Geology. Paleozoic Era. Geol. Wis. Survey of 1873-1879, vol. 1, 1883, -

go ae SNE Fe ee Peay OO ae Lec iy ae ee ee
Vitis’ | bp ebe Seek ery. THE CAMBRIAN, ie fun

shore of Lake Superior. He considered they probably. indicated the —

aes Eingulapts cies Doe p. 127, Fig. 13, f es Pgh ee ee
Obolella polita, Hall, p. 127, Fig. 13, h. Ed 4 art fi
Orthis pepina, Hall, p. 127, Fig. 13, i,j, k, 1.
Triplesia primordialis, Whitfield, p. 127,Fig. 13, m.
Leptxna barabuensis, Winchell, p. 127, Fig. 13, n, o.
Arenicolites woodi, Whitfield, p. 128, Fig. 14, a, b.
Dikelocephalus sp. ?, p. 129, Fig. 15.
lodensis, Whitfield, p. 130, Fig. 16, a, b.
pepinensis, Hall, p. 130, Fig. 16,c,d,e,f. : ae
Aglaspis eatoni, Whitfield, p. 130, Fig. 16, g. . ees
Chariocephalus whitfieldi, Hall, p. 130, Fig. 16, h.
Arionellus convexus, Whitfield, p. 130, Fig. 16, i.
Ptychaspis minuta, Whitfield, p. 130, Fig. 16, j, k.
Ileznurus quadratus, Hall, p. 130, Fig. 16,1, m, n, 0, p. — =
Crepicephalus gibbsi, Whitfield, p. 130, Fig. 16, q. ‘t J
Conocephalites wisconsensis, Owen, p. 131, Fig. 17, a, b, ¢. * “i
calymenoides, Whitfield, p. 131, Fig. 17, d. y >
Agnostus josepha, Hall, p. 121, Fig. 17, e, f. : 7
Ellipsocephalus curtus, Whitfield, p- 131, Fig.17,g. - %
Agraulos woosteri, Whitfield, p. 131, Fig. 17, h, i. ce
- Pemphigaspis bullata Hall, p. 131, Fig. 17, j. e
Climactichnites youngi, Chamberlin, p. 132, Fig. 18.
fosteri Chamberlin, p. 132, Fig. 18. — ng +f

The species Orthis remnichia and O. sandbergi are described in | 1886 .
by Prof. N. H. Winchell from the St. Croix sandstone.! atae :

In 1890, Mr. C D. Walcott described the inllowing species from the
Upper Gambrian of Wisconsin and Minnesota :?

Metoptoma? minneiskensis, p. 267.
? peracuta, p. 267. : .
Conularia cambria, p. 270. aan
Spirodentalium, n. gen., p. 271. : ;
-Spirodentalium osceola, p. 271. -
_Ptychoparia connata, p. 272. > > ae
pero, p. 274. . ey .
Agraulos? thea, p. 277. ‘ RAs

(43455

-

RED SANDSTONE OF LAKE SUPERIOR.

On Pl. 1 ¢ and U1, Figs. 1 and 2 of the illustrations in the Geological
Report of Wisconsin, Iowa, and Minnesota, 1852, Dr. D. D. Owen fig- —
ures certain markings he observed on similabnsian? from the northwest — a
remains of fossil sea-weeds or fucoids. ee

There is a specimen in the collections of the National Museum, la
beled “‘ Plants of Lake Superior, D. D. Owen.” The specimen looka@
very much like the sandstones of the interior of Wisconsin, and is cov- —
ered with casts of annelid trails, more or less crushed and matted down, —
which gives a resemblance to fucoiis, Of traces of life other than that
of annelid trails and borings nothing has to my knowledge been made
known to the scientific world. | | eee

1 New species of fossils. 14th Ann. Rep. Minn. Geol. Nat. Hist. Surv., 1886, pp. S1T-S48- FPS aw
? Description of new forms of Upper Cambrian fossils. U.S, Nat. Mus. Proc., ies 1, 1899, pp. 267: 270,

*,

‘HASTERN BORDER OR ADIRONDACK SUB-PROVINCE.

+ ‘he. first notice of anything of an organic nature in the strata now
rred to the Potsdam or Upper Cambrian zone, about the Adiron-
(8, was by Mr. J. H. Steele in 1825, who described certain large cal-
eous concretions.? These were subsequently described in detail by
f. J. Hall and named Cryptozoon proliferum.®

ithe second notice is by Dr. E. Emmons, who states that near Keese-
e, in the bottom of the fissure at the high bridge, he found numerous
cimens of small bivalve mollusca, a lingula.

~ Lingula acuminata was described by Mr. T. A. Conrad as ES
in the Calciferous sandrock, and in the table of classification he places

‘ranklin County, New York.

2 Inhis description of the Potsdam sandstone at Au Sable Chasm, Jef-
fe rson County, New York, Dr. Emmons figures and names Tihireta
ant tiqua.s The same woadout is used by Prof. Hall to illustrate Lingula
cuminata of Conrad.’

In volume I of the Paleontology of New York, Prof. J. Hall defines
e genus Scolithus of Haldeman (p. 2), and describes 8S. linearis
ideman (p. 2); Lingula prima of Conrad is described and illustrated ;
and Lingula antiqua is proposed as a new species for the specimen fig-
a ired by Emmons as Lingula antiqua (p. 3). These species are illustrated

on Plate 1.2 -

F .ttention was called to the presence of a track and footprint of an
mal i in the Potsdam sandstone of Lower Canada by Sir W. EK. Logan

Notice of a new brachiopod from the lead. bearing rocks at Mine la Motte, Missouri. Phila, Acad.
Sel, Proc., vol. 23, 1871, p.-185.
A description of the Oolitic formation lately discovered in the county of Saratoga, and State of New
. Am. Jour. Sci., vol. 9, 1825, pp. 16-19.
4 Megctonoen, » gen., Cryptozoon proliferum,n.sp. Description of Pl. vi. 36th Ann. Rep. State
Mu: Nat. Hist., 1884.

eport of the geologist of the 2d geological district of New York. Second annual report of the
ogical Survey of N.Y. Albany, 1838, p. 230.
econd annual report of the paleontological department of the survey, Third annual report of
re » Geological Survey of New York. Albany, 1839, pp. 63, 64.

Geology of New York, Part 2, comprising the survey of the 2d geological (northern) district.
2 digical survey of New York; its influence on the productive pursuits of the community. N.
le Agric. Soc. Trans., for 1843, 1844, p. 252.
rae. of New ork vol. 1, containing bec prs of the organic remains of the lower

a"

5 Coa as) he “ xy ne ae 4,
a % Sa Penta or ach 20S - ] i et my ie ee ~
: 25 = * Rt he ~ 2. ti 4 = 4 s ». ca sag aay!
ahd y A * - 4 iG? ae er mS \
230° ay & THE CAMBRIAN. UI TGR ov, Sa
“
,

_._ the Potsdam sandstone in New York and Pennsylvania and as far as Tennessee. a

in 1851. He described its mode of occurrence and sti GeeapWie' posi -
tion.! This paper was followed by one by Prof. Owen, sas refers the
tracks to a species of tortoise.”

At a meeting of the British Association for the Advancement
‘Science, held at Ipswich in 1851, Sir W. E. Logan exhibited a slab of
sandstone and a cast from a fannae one, showing what Prof. Owen had,
in a communication to the Geological Society, pronounced to be a track
and footsteps of a species of tortoise, thus proving the existence o of
reptiles at the very earliest period of knewn animal life? ~ | an

In describing in 1852 the sandstone occurring in Beauharnois County,
_ Canada, Sir W. EK. Logan makes the following observation upon Sco-
~ lithus linearis :* cae

ae ay

a
3S
of

In this part it [the sandstone] is abundantly marked over ‘pesslicea bis surfaces by y
what the geologists of New York have called Scolithus linearis, which consists, where
the rock is weathered, of straight, vertical cylindrical holes, of about an eighth of. an
inch in diameter, descending several inches, and where the rock is unweathered of
corresponding solid cylinders, composed apparently of grains of sand, cemented by :
a slightly caleareous matrix, more or less tinged with peroxide of iron. Mr. Ha We
and other American geologists include them among the Fucoids of the rock, but th ey
appear to me more like worm holes. In one or two instances I have perceived the ub
the tubes are interrupted in their upward course by a thin layer of sand, of a por
tion which descends into them and stops them up; and from this it would appear
that the cylinders were hollow when the superincumbent sand was spread over ther a.
Whatever may be the origin of the tubes, they strongly mark many beds in the upp
part of the sandstone throughout the Canadian portions of its distribution aneady
mentioned; and it is stated by Mr. Hall that the same characteristic accompanie

He also speaks of the presence of Fucoides and of Lingu la antiqua.
This is followed by a detailed account of the strata containing the foot-
prints described in the same volume by Prof. Owen. 7 7

This paper by Mr. Logan was followed by one by Prof. Owen, who
described the various footprints and impressions under the following y
names :> S

Protichnites septem-notatus, p. 214. _
Protichnites octo-notatus, p. 217.

latus, p. 218.

multinotatus, p. 219.

lineatus, p. 220.

alternans, p. 221.

. "’

The descriptions are accompanied by admirable iliuetations of ‘the
varieties designated. He concludes that the im pliers appear to. have
been made by animals allied to Limulus.®

-10On the occurrence of a track and footprints of an animal in the Potsdam sandstone of L
Canada. Quart. Jour. Geol. Soc., London, vol. 7, 1851, pp. 247-250. >a

. 2 Lbhid., p. 250-252. ~ Ha

Qn the age of the copper-bearing rocks of Lake Superior and Haron: ote. British Assoc

- Trans., of sections for 1851~’52, p. 62.

4On the footprints occurring in the Potsdam sandstone of Canada. Quart. Jour. Geol. Soo. Te “4

Proc., vo). 8, 1852, pp. 200, 201. , ;
5 Description of the impressions and footprints of the Protichnites from the Potsdam sandstc on

Canada. Quart. Jour. Geol. Soc. London, vol. 8, 1852, a ais : ot ae

6 Op. cit., p. 224. ; ae Mertens

“? a F fone RS = a iA Se Ames é ¥ 7 a :
Ot Cee OT ee el = es eae Eee By, a te
eS eS e eeey, * ee bon hole aes 243 Cog pet, Hanes

Be: “Cape * _PALEONTOLOGY—ADIRONDACK.
“10 1856 Dr Geimions published a desctipiion of Lingula prima Em-
mc ons, SL la antiquata Emmons, and L. acuminata Conrad. The two

atter species are illustrated on Pl. Ivy, but in the description of the
ple ate | the figure of Lingula antiquata is called L. prima by error.’
In 1860, Prof. F. H. Bradley described and illustrated Conocephalites

.<.

n vinutus from the Potsdam sandstone at Au Sable Cha sm, near Keese-
ville, New York.’
2 The announcement of the discovery of another type of track in the

Pot: sdam sandstone was made by Sir W. E. Logan, in 1860. For this
he Eiraposed the name Climactichnites wilsoni.°

In 1869 Prof. O. C. Marsh described a new species of Protichnites
from the Potsdam sandstone of Essex County, New York, naming it
otichnites logananus.‘

_ As the result of comparative study of different tracks, Dr. J. W.

3 Limuloid crustacean.

= collections made at Keeseville, New York, Messrs. Hall and
Ww Pea described the genus Paleacmea, the type species being
Paleac wa typica and Hyolithes gibbosa.®

eae n 187 Mr, E. J. Chapman says that the fossil tracks known as Pro-
i ichnites and Climactichnites are of such a nature that he does not con-

x more than impressions of large fucoids. If this idea be accepted
Riponcs to change the names to Protichnides and Climactich-
ni ides.” ~- - :

Bi: ‘rom the limestone in Saratoga ase, Now York, in which Mr. J.
ac escribed in 1879 the following species : °
" = _ Platyceras minutissimum, p. 129,

. _ Metoptoma cornutiforme, p. 129.
Conocephalites calciferus, p. 129.
Conocephalites harttii, p. 130.

‘ 5 Ptychaspis spéciosus, p. 131.

ie presence of a species closely allied to Bathyurus armatus of Bil-
ings was noticed ; also Stromatopora sp.?, Lingula acuminata, Metop-

Tne

4 ny A merican Sediosy. containing a full statement of the principles of the science, with full ilustra-
ms of the characteristic American fossils, Albany, 1856, vol. 1, pt.2, pp. 292, 203.

‘ ee cription of a new trilobite from the Potsdam sandstone. Am. Jour. Sci., 2d ser., vol. 30, 1860,

‘< gh track of an animal lately found in the Potsdam formation. Canadian Nat., vol. 5, 1860, pp.

patel bur. Sci., 3d ser., vol. 5, 1873, p. 17.
lice of two new species of fossil shells from the Potsdam sandstone of New York. 23d Rep.
z York State Mus. Nat. Hist., 1873, p. 242.
‘the probable nature of the supposed foss%. tracks known as Protichnites and Climactichnites.
f an Jour. Sci., Lit. and Hist., new series, vol. 15, 1877, p 490.
iptions of new species of fossils oe the Calciferous formation. ‘324 Rep. N. ¥Y. State Mus.
cba PP. 129-131. _

_ =

a oe 2 ES ar es

awson concluded that Protichnites of Owen was possibly made by

ler ‘em to be of animal origin; and he suggests that they are noth--

. Steele noticed the large concentric Pee On) Mr. C. D. Walcott

— tion. This reference was corrected in 1884.1

from the Potsdam sandstone of Buckingham, Quebec, Messrs. Ami an

_ principally in the preservation, S. canadensis occurring in hollow tubes

OT eS PI re ne st ee Se age Ee Ot OS SEP ers
¥ * > ae “* a ee i 1 mae +f akathe - x i * ¥ tt i Toe, S 3 na
ee - ¥ ; = Sgr = Ms
ae ‘THE, CANBRIAN. eee
aed 7s

a

Wisconsin, although the ‘rocks were referred to dhe Caleiferous form me

In 1883, Mr. W. F. Ferrier called attention to the presence of track:
on the Potsdam sandstone at the head of Au Sable Chasm in Basex
County, New York. They were referred to the genus Gyrichnites 0
Whiteaves.? Later the tracks discovered by Mr. Ferrier were made th he
subject of a note by Sir J. W. Dawson, who proposed the pine nan n 6
of Clydichnites fer them.* |

In a note on some obscure organisms in the roofing slates of Waele he
ington County, New York, Prof. James Hall redescribes bythe
asteroides Fitch as Dacty yloidites bulbosus.‘

A revision of the fauna occurring in the limestone beds of Saratonll ;
County was made by Mr. C. D. Walcott in 1886, and the seaecmits / lis t
was published : 4 i ‘

E

5 NEW YORK. WISCONSIN.
*Cryptozoa prodiferams os seen Ded ceeds Cobden soe ab eee bhiced met
Lingulepis acuminata....... eevee | Lingulepis pinnzeformis,
Platyceras minutissimum........-. Platyceras minutissimum.,
es Platyceras hoyti- ...--..-- 2-0 secon ee teens cane cee n ees tn eee “
Metoptoma cornutiforme...........Metoptoma cornutiforme.
SLUNIOT SF ..c'S ac as > bale bend oie ke. pk nakel s Sees se eee eee °
Billingsia saratogensis..2 25. 1-22. beecets sp ocaedsauuele sabe Seah
Matthevia variabilig:. 12. o25.3.. Wo obscene es Se iiedes Capek
Dicellocephalus hartti............. Dikelogaphilia pepinensis.
BUC CIOMUG. (0's cstnl oingin'= Kepner ee lodensis.
Ptychoparia calcifera..........-..- Ptychoparia wisconsensis.
CR) -saEa logpensit <0 see. clan wees oweni (of Hall).

As the result of the comparison of an extended series of specimens

Sowter concluded that Scolithus linearis and S. canadensis were ‘den
tical species; the main differences existing between the two bein, 1g

or burrows, while S. linearis occurs as casts of the interiors of burrow W 3
or holes.®

In 1890 Mr. C. D. Walcott described? the following species ‘froma the
limestone in the vicinity of Saratoga Springs, New York: 3

Platyceras hoyti, p. 268.
Trochus? saratogensis, p. 268.
Agraulos saratogensis, p. 276.

1 Potsdam fauna at Saratoga, New York. Science, vol. 3, 1884, pp. 136, 137.
2 Notes on a fossil track from the Potsdam sandstone of northern New York State. Canadian Nat
new ser., vol. 10, 1883, pp. 466, 467. ~~ _
3Impressions on Potsdam sandstone. Science, vol. 1, 1883, p. 177. : .
4 Note on some obscure organisms in the roofing slates of Washington County, New York.
Rep. N. Y. State Mus. Nat. Hist., 1886, p. 160, pl. 11, fig.1,2. ~
5 Second contribution to the studies of the Cambrian faunas of North America. v. 8. Geol. Sur
Bull. No. 30, 1886, p. 21.
6 Report of the geological branch fof Uttawa Field Naturalists’ club}. ‘Ottawa Naturalist, ve 0
1887, pp. 96, 97.
id ” Description of new forms of Upper Cambrian fossils. U. jie Nat. Mus. ap Pree, ” he 18, 1800, PP. 27

ia)
° &z “ “ At ae $. + Sages! “ae
PERS 6 i ah

~~. Pron,

=-

> eae

a a atin sbi Sieaars. Meek and paves to Lieut. G. K. Warren,
dated February 8, 1858, attention is called to the identification of fos-
from a sandstone in the Black Hills equivalent to the Potsdam sand-
a ‘one. of the New York series. They recognized Lingula, Obolus?, and
fre sments of trilobites, belonging to species known to occur in the
Potsdam formation in Wisconsin and Minnesota.! This notice was fol-
4 te owed i in 1861 by the publication of the first description of the Cambrian
fauna of the Rocky Mountains. The new species described but not
a ustrated include Obolella MORE Theca (Pugiunculus) gregaria, and
Arionellus (Orepicephalus) owem.” The descriptions of the species were
e re published i in 1862, in the American Journal of Science, in connection
with figures illustrating them. The last species is described as Ario-
ells? owent. ‘There were also identified from the same horizon Langula
ry pr rima Conrad and Lingula antigua Hall.’

Hayden in 1864, in their account of the paleontology of the Upper Mis-
E ‘souri. Lingula antiqua, mentioned in their letter of 1858, is identified as
EL ingulepis pinnaformis Owen (p. 2), and the name L. dakotensis proposed |
a the event of the shell being subsequently determined to be a new
Spe acies (p.3). A description and illustration is also given of Lingulepis
prima Conrad (p. 3), Obolella nana, M. & H. (p. 4), Theca gregaria, M.
oH . (p. 5), Ayraulos owen, M. & H. (p. 9) = tirtonetis (Crepicephalus)
3 oweni, of the paper of 1861), and an sicdatcomined species of Agraulos —
5 10). All of the species are referred to the Potsdam or Primordial
ndstone.t
In 1876, when reporting upon the fossils collected by Captain Lud-
Fig, DW's, expedition to the Yellowstone National Park, Prof. Rk. P. Whit-
fi ield deseribed two species that are now referred to the Upper Cambrian
ae Z0ne, Orepicephalus (Loganellus) montanensis and Arionellus tripune-
ta aius, referring them to the limestone of the Pot&Sdam group overlying
pee quartzite near Camp Baker.°
A preliminary report on the paleontology of the Black Hills by Prof.
R . P. Whitfield contains a description of Palwochorda prima, Paleophy-
| 7. cus occidentalis, Lingulepis cuneolus, L. perattenuatus Crepicephalus (Lo-
_ganellus) centralis, and C.(L.) planus. All of these species are referred

__ 1 Fossils of Nebraska. Letter from F. B. Meek ani F.V. Hayden. Am. Jour. Sci., 2d ser., xols2y,
ey 858, p. 439.
a 2 Descriptions of new Lower Silurian (Primordial), Jurassic, Cretaceous, aud Tertiary fossils, col-
5. ected in Nebraska, with some remarks on the rocks from which they were obtained. Phil. Acad. Sci.,
Proc. vol. 13, 1861, pp. 435, 436.
g *The Primordial Sandstone of the Rocky Mountains in the Northwestern Territories of the United
=) bates. Am. Jour. Sci., 2d ser., yol. 33, 1862, pp. 78, 74.
ct Palcontology ‘of the Upper Missouri; a report upon collections made principally by the expeditions
te md er command of Lieut. G. K. Warren in 1855-’56. Invertebrates. Smithsonian Contributions No.
eet pp. 1-10. -
; Descriptions of new species of fossils. Report of a reconnaissance from Carroll, Montana Terr.,

rm) BN. __-PALRONTOLOGY—DaxoTA | 233°

3 The Black Hills fauna was again described by Messrs. Meek and

pe Missouri, téthe Yellowstone Park and return, made in the summer of 1875 by Wm. ~

: ~

_ report are illustrated, and aasabip tis and illustrations given of Pal
ophycus sp. undet., Arenocolites sp. undet. (p. 333), Lingulepis pinna-

- remarks to the paper it is stated that the horizon of the Potsdam forma t

Wisconsin.’

~ 1886, p. 60. =

ota ae oes eas RRA Ps it Sees Fe
4 ee 'é : Tee : x =

AL * mi } EP ab Be eS : ~

934 eee | as THE ‘CANBRIAN Res at

J ~ ety one Ree

to the Pataiam feitoradtiat of the Black Hiils of Dakota. . tr the final a
- port, which appeared in 1880, the species described i in the prelimi U

formis {p. 331), Lingulepis dakotentis (p. 337), Obolus? pectenoides (p.
$38), Obolella polita (p. 339), Obolella nana (p. 340). In the prelimina ary

tion of the Black Hills appears to be, so far as the fossils will serve to
determine, about the same as that of Wisconsin and the neighbori
States.” :

The only fossils of the Cambrian fauna identified in Colorado are
species of Dikelocephalus from Quandary Peak of the Mosquito Rangel :
and the Lingulepis found in the Trout Creek section (p. 62). a

In 1890 Mr, C. D. Walcott* described three species from the Upper
Cambrian of the Black Hills of Dakota. They were Hypolithes newtona
_ (p. 270), Diyehopares vacuna (p. 275), and P. (Liostracus) panope (P. 275),

TEXAS. ; peties . — 2
; ; = :. Fag
The first notice of the presence of a fauna in Texas subsequently
assigned to the Cambrian is by Dr. Roemer 1 in 1849. A description | of
Lingula acutangula (p. 420) and Pterocephalia sancti-sabe (p. 421) is gives n
by him in that year without illustrations.°
* In his more extended work on the geology of central’ Texas he ¢
scribes and illustrates Lingula acutangula (p. 90), Pter ocephalia sancti
sabe (pp. 92, 93), and the genus Pterocephalia (p. 93). He also illt 18+
trates the ane of a trilobite, allied to Arionellus, and the pygidium of of
another species, on Table x1.° 4
The primordial character of the fauna referred to the Silurian by Dr 2
Roemer was announced by M. J. Barrande the following year. He
compared it with the fauna of the Potsdam sandstone of New York a ant nd

As geologist of the State of ria Dr. B. F. Sha wante: described a
1861, the strata referred to the Potsdam sandstone. Of the fossils col -
lected he describes as new; Zz a

; Agnostus coloradoensis, p. 218.
Arionellus (Bathyurus) texanus, p. 218.
planus, p. 219.

a

1Preliminary report on the Paleontology of the Black Hills. U.S. Geol. and Geog. jah of the ies ey
Mountain region, 1877, pp. 7-11. 4
; 2Paleontology of the Black Hills of Dakota. Report on the geology and resources of the Black B Hills |
-of Dakota, 1880, pp. 329-344. * 3 ig 4
* Geology and Mining Industry of Leadville, Calera? U.S. Geol. nee Monograph vol. 12, pt. 1,

_ ‘Description of new forms of Upper Cambrian fossils. U.S S. Nat. Mus. Proc., vol, 13, 1890, pp, 2 7 7 3
279. 3
6Texas. Mit besonderer Riicksicht auf deutsche Leaewton und die physischen Verhiiltniss
des Landes nach eigener Beobachtung geschildert. Bonn, 1849, pp. 420-421.
® Die Kreidebildungen von Texas und ihre organischen RinwoWtuaac. Bonn, 1852.
7 (Silur-Gebilde in Texas und am Oberen See.) Neues Jahrbuch fiir Miner, 1853, , PP. 446, at.

ee

1¥ Rae = ie " Pe eS 5 xg Pip *, « ae toes ae aS cs Wee ms INCE RE aE
ae " PaLRoNtoLocy—mExas AND “ARIZONA. 235
a8 on ;

Ce nocephalites aaa p. 219, 3
2 - pbillingsi, p. 220. ~
| eae roemeri, p. 220.

_. Discina microscopica, p. 221.

i

Ihe mentions Camerella sp. ?, and Dapuitis sp. ? (p. 221).! He cor-
Sthis fauna with base provisionally designated as 4%: a very

% ‘In the polcotictia obtained by Mr. C. D. Walcott in his reconnais-
S: ance of the central area of Texas the following species have been
id au tified :

Peiepanites. sp.? Ptychoparia occidens, Walcott.
Lingula acuminata, Conrad. affinis, Walcott.

perattenuata, Whitf. burnetensis, Walcott.
Obolella polita, Hall. | llanoensis, Walcott.
_ Triplesia primordialis, Whitf. ? metra, Walcott.
- Orthis coloradoensis, Shumard. pero, Walcott.

- remnichia, Winchell. ? urania, Walcott.
Platyceras texanum, Walcott. similis, Walcott.
‘Bellerophon antiquatus, Whitf. _patersoni, Hall.

_ Dikelocephalus minnesotensis, perseus var., Hall.
Owen (?). wisconsensis, Owen,
belli, Billings. ~~. Agraulos convexus, Whitf.

_ Ptychaspis granulosa, Owen. Agraulos ? sp. ?

- Chariocephalustumifrons, H. & W. Illenurus dia, Walcott.

,

a es fauna will be illustrated in connection with a review of the Up-
. per. Cambrian fauna of North America now in course of preparation.
In 1890 Mr. Walcott? described the following new species from RP
pe yer Cambrian strata of Burnet and Llano Counties:

‘-
Picivooras texanum, p. 268,

Ptychoparia burnetensis, p. 272.
llanoensis, p. 272.

? metra, p. 273.

pero, p. 274.

? urania, p. 274.

- Tileenurus ? dia., p. 277.

oa
! =
, : >

a ARIZONA.

The paleontologic work on the Cambrian fauna found in Arizona has,
th S$ far, been confined to the identification of the species discovered
in the Tonto formation of the Grand Caiion. A preliminary study of
the fauna has been made and drawings prepared of the species, but up
to the present time nothing has been published in relation to them.

BY The Primordial zone of Texas, with ‘descriptions of new fossils. Am, Jour. Sci. 2d ser., vol. 32,
186), pp. 213-221.

e cit., pp. 217, 218. :

3 <t Resaaea of new forms of Upper Cambrian fossils. U.S. Nat. Mus. Proc., vol. 13, 1890, pp. 267-279.

‘ f=

= by)

YH RR Lae ae. Ree ee ES - Ses Ping St
POE Te AR rea he, See give aS Pe a ee eet Se eae Oe agen ee
ae t wy) » > , 5 oF “fl 5 mh ~ vf > a “Se 7)
Ss om ee oe ae oa = nat Dols on ao a e ak ee mes re
A et Say “5 5 Se ee ther ts te :
(eee te fe Sage a = hs OP ‘2
~ ok = ee ney <
- 4 = 2 *% > '
hs : UO!
a e fees 7 ne ata on
4 Z S 4 > .* ee 9S
, ea ve Le a
< - Tre eee
> 2 ae.
~ - % 2 x as
+ a x
- “at —s

the scientific world gives that term a standing that even the claims of

occur, and it is therefore impossible for any one geologic province to
afford a nomenclature that is applicable to the geologic provinces: of
the entire world or to the entire geologic series. a

;, applied to the groupings of the Faiviivatione: but, if practicable, the

Dutchess County limestone are lithologically distinet formations, but t
they are grouped under the Upper Ceniee terrane asa pornos ot
the Cambrian group. ‘ a ee

CHAPTERIII.

NOMENCLATURE EMPLOYED IN THE DESCRIPTION OF THE FOR
MATIONS. oe

Several considerations are to be borne in mind rejaiee: to geolc sic
nomenclature : | 4

(a) The name in itself is nothing unless it conveys to the mind @
Sess impression of what it refers to and enables the student to make a »
correlation between its entity and some other: entity that has another
terminology. ad

(b) Priovity of discovery and naming should be sustained by the proof
of the accuracy of the original observations, the latter to be judged b b ;
the testimony of the formations in the areas where they were first: made. a.
If the original proposer of a name bases it upon such errors of observa a-
tion and interpretation that subsequent observers can not verify b nis
work, and the name can be used only by dropping a name proposed 2 5
the faut of accurate observation and definition, the latter should — be
retained and the law of priority should not be used to bolster up an-in-
definite term. =a

(c) Long use of, and the general acceptance of, a well defined tern’ by

half understood, badly defined term supported by priority shoud n t
displace. This may be called the law of usage. er:

(d) From the fact that all the strata of the geologic series do Be K-
ist in any one geologic province and that unconformities between diffe i
ent portions of them are not contemporaneous in all provinces, it neces
sarily follows that the rock series of any one geologic province can not
possibly be the chronological equivalent of the rock series of othe or
provinces. Overlappings of series of different chronologie age must

(e) Each geologic province should have a nomenclature denoting by by
name each formation contained in it and, if necessary, the names to be

Vo

formations and the grouping of formations phaula be referred to so me 2
position within the larger composite groups. For instance, the Pot: [S-
dam standstone of New York, the Saratoga County limestone, and the @

236 - inn Sign Se a

MS Pere eS if Tp . Sin at
mr) pa. “sak _Mometarone—ousean, - 237

: inces that can not hig 2 ele to be identical or synchronous.
; ) The : study of the serial relations among rocks by the modern
hod is of as much importance as that of the specific relations of dis-
inct horizons or of particular formations. The serial relations of one
eries of rocks in one province can be compared with the serial relations of
ane her group in another province ; but the two should receive separate
names and be grouped under the greater series to which they belong.
Fo instance, the Trenton series of New York may be compared with
» Lebanon. series of Tennessee and united as a portion of the Lower
Silurian (Ordovician) and respectively compared with the same portion

of the Lower Silurian (Ordovician).

iti pe to remove portions of cee aces Giben terranes, or groups
3 still Zhe the original name, if rhe portion remaining is distinct or

CAMBRIAN.

4 “4 ‘he term Cambrian was first introduced to the attention of geologists
at the Dublin meeting of the British Association for the Advancement

. gwick and R. I. Murchison, entitled ‘On the Silurian and Cam-
brian Systems, exhibiting the order in which the older sedimentary
; ata succeed each other in England and Wales.” An abstract of this
16 r appeared i in the account of the proceedings of the British Asso-
ion published in the Edinburgh New Philosophical Journal for
il-October, 1835, page 390. In this the name Cambrian is spelled
abrian, probably by a typographical error. The paper appeared in
in 1 volume 5 of the usa of ue Association. In the account of

= in the alle of England and some portions of north Wales, in consequence of
entire want of continuity between the Carboniferous series and the interior schis-
. * * * Prof. Sedgwick then described in descending order the group

‘nante of Upper Cambrian group. It occupies the greatest part of the chain of the

‘ me where it is connected with the Llandeilo flags of the Silurian system, and
=F = cP:

f Science in August, 1835. A joint paper was read by Prof. Adam

ae” ee. - od
Sipe aes

la re hy > : ey ia : aw is ne sas é 5 atu ae: re oe = nei laa "
(oe Me Reha), THe CAMBRIAN. Sepia Lc as twuks
a ~ - ‘ - ay" << ar, ae ® ~ e
. . c ; ,

te

is thence expanded through a etiabeabie artaae of esi ‘Wales, ‘Th. ‘one par ; of
its course it is based on beds of limestone and calcareous slate, but on the whole it
_ contains less calcareous matter than the Silurian system and has fewer organic
remains. Beds of good roofing slate occur, and a perfect slaty cleavage is is oft en
observed in it transverse to the stratitication, but other parts of it are of a coarse
inechanical texture. To the next inferior group he gave the name of Middle Can
brian. It composes all the higher mountains of Caernarvonshire and Morionethabigtl BD,
and abounds in fine roofing slate, alternating with and apparently passing into ir-
regularly interstratified masses of porphyry. Some portions of it are coarse and me-
chanical, and it contains (for example at the top of Snowdon) a few organic remait ns
auda te samples of highly calcareous slates, but no continuous beds of limestone.
The same group, with the same mineral structure, and in the same position, but wit th
out orgauic remains, is greatly developed in Cumberland, The Lower Cambri ian
group occupies the southwest coast of Caernarvonshire and a considerable portion | of
Anglesea; it consists chiefly of chlorite schist, passing here and there into mica schist
and slaty quartz rock and contains subordinate masses of serpentine and white gra: ne
ular limestone. It contains no organic remains. wi ~~
In this first description, Arckean rocks are included in the lower or
division; the Middle Cambrian embraces the roofing slates, and the
Onivbrian group as now general] y accepted; while the Upper Cambria
included much of the Lower Silurian of Sir R. L sprees or ue
- Ordovician of Prof. Charles Lapworth. hm
At a meeting of the Geological Society of fonda’ in the spring 0 of
1838, Prof. Sedgwick read a paper entitled “A Synopsis of the Englis sh
series of stratified rocks inferior to the Old Red sandstone, with
attempt to determine the successive natural groups and formations.”!
When describing the sections of North Wales, etc., the chlorite slates,
| quartz rock, and mica slates of Anglesea and ‘Guatbarvonshe are no rt,
included in the Cambrian as was done in 1835.22. The Lower Cambrian
system includes the old slate series of Caernarvonshire and Merionet h-
shire, and ends with the calcareous beds, which range from Bala to the
neighborhood of Dinas Mowddy. 4
The next group, the Upper Cambrian series, commences with the fossiliferous h beds
of Bala. It includes ali the higher portion of the Berwyns, ae all the slate rocks
of South Wales, which are below the Silurian system, * * ‘Many of the fossil 1s
are identical in species with those of the lower division of the Silurian system, nor
have the true distinctive zoological characters of the group been well ascertained.
In this arrangement, the Lower Cambrian of 1835 is referred to the
primary stratified group, to which he Boxe the provisional name of Pro- !
tozoic.? | a
Tt is further stated that at the worth end of the Berwyn chain th @
Upper Cambrian appears to pass by insensible gradations into the
lower division of the upper system, the Caradoc sandstone. Prof.
_ Sed gwick does not appear to have been aware at this time that his Bala
series was a portion of Murchison’s Lower Silurian, as hoses sito, by the
| latter in 1835. es:
Many geologists have insisted upon restricting the Canibeien to the
Lower Cambrian of the scheme of 1835, which Prof, Sedgwick cut off

1 Proc. Geol. Soc., London, vol. 2, 1838, pp. 675-685. 2Op. cit., p. 685. 8 Op. cit., p. cs

as

ie

i Ase nS Bes,
if ee NOMENCLATURE—CAMBRIAN. . 239 :

e ar. one ‘It is also well to notice that the Cambrian of
) udes exactly the same representative formations as Emmons’s
ic System of 1842-1860, or the Cambrian and Lower Silurian
svician) | as now known.
In 1852 we find the Lower Cambrian divided into the Festiniog group
D0¥ » and the Bangor below. The Bangor group is composed of the
nherris slates and Harlech grits; and the Festiniog group of the
Rts flags, Tremadoe slates, and Arenig slates ard porphyry, the
hol » having a thickness of 10,000 feet. The Upper Cambrian includes
Bala group, which was Atidea into the Lower and Upper Bala,
a thickness of 8,000 feet. Above this the Caradoc sandstone,
: estone, and shale of the Silurian occur with a thickness of 1,500
i Pcie paper on the Caradoc sandstone of Shropshire, by Messrs. J.
Vv. . Salter and W. T. Aveline, it is stated that the fossils of the supposed
ypical Caradoc sandstone are identical in species, and in association
eeenntiate numbers of the prevailing species, with those of the
group; and there is no admixture of other or new forms, or of
ies’ characterietic of higher parts of the system.? By priority of
efinition and description, the Llandeilo and Caradoc beds belong to
fur chison’s Silurian system; and the Bala series of Sedgwick are
ra atigraphically and paleontologically the equivalents of the Llandeilo
i Caradoc series. They were fairly removed from the Cambrian
= tem by the work of Messrs. Murchison, Sedgwick, and Salter; and
n 18 354 the Cambrian system included of the artnet Gimbireen the
ic idle member only, the lower division having been removed by Prof.
dgwick in 1838. The distinguished founder of the Cambrian system
-¥ 1 not admit the exclusion of the Bala series from the Cambrian, but
ith all the facts assembled, as in a recent paper by Prof. J. D. Dana,’ I
ri) ink we are Nos oli to restrict the Cambrian to the original middle

e last tabulation given by Prof. Sedgwick of his Cambrian system
est in the preface of Mr. J. W. Salter’s Catalogue of Cambrian
1 Silurian Fossils in 1873, as follows: 4

Upper Bala.

re
a
a ad
<d
=

Middle Bala.

Lower Bala.

Arenig or Skiddaw.
‘ Tremadoc.

Middle ...-- Ffestiniog.

Menevian.

Harlech,

Bangor.

Longmynd.

Llanberris.

Cambrian:

hic Geol. Soc., London, vol. 8, 1852, p. 147.

the “Caradoc Sandstone” of Shropshire. Quart. Jour. Geol. Soc., London, vol. 10, 1853, p. 63.
zwick and Murchison ; Cambrian and Silurian ; Am. Jour. Sci., 3d ser., vol. 39, 1890, pp. 167-180.
e classification of the Cambrian rocks). “ Preface to a Catalogue of the Collection of Cam,
nd J Sitnvian fossils contained inthe Geological Museum of the University of Cambridge,” by Jd

EERE TESS ig ee ee eR

~

7s

p=

eee a i ag pas te PR PN Tw Se, PS nese BB Fo, By ROO ne hg
a, ase: os b - ~ + Se ~ as Sire A a Sk RS aed sets af"
a " - T.2-4 ee ee SES: Ste
"B40. 2 Z sea "THE CAMBRIA. © oe ee

~ gon’s Siluria, and also the observations of Prof. Sedgwick on the Cam.

' waeke, slate, limestone, ete. All this country, according to the views of Murchison |

-nessee with that of Wales entirely upon its lithologic characters andy

~ lower masses which I considered as equivalent to the Taconic rocks; the Lower .

_ quartz be found wanting, it only proves the absence of that development which is so ~

entirely ignoring Cambrian except to state that it was equivalent to sal

. ?
ee r rs, oP eee

With Ne exception 0 of the Bala and Arenig series the paystem is es se n-

the foank day. ¥
As geologist of Tennessee, Dr. Gerard. ‘Troost read Sir R. I. Murehi-

- brian rocks of Wales. Discussing the changes in nomenclature made_
necessary in pEeeeee the views of Messrs. Murchison and Sedgwick,
he says in 1841: | |

After having BE CAF in my last report, the line of junction of the crhmareia 4

or crystalline rocks in East Tennessee, I mentioned that the country west of the line
which separates Tennessee from the State of North Carolina is composed of gray- )

e

and Sedgwick, belongs to a new division, which they call the Cambrian system. A ;

He then proceeds to describe the geographie distribution of the rock S
that he referred to the Cambrian sy stem, identifying the series in Ten-
the absence of organic remains, and from the fact of its being suc. 4
ceeded by a series of limestones from which he obtained and identified

Silurian fossils. > a
The presence of the equivalent of the Cambrian system in Ameriea
was clearly recognized by Dr. E. Emmons, who, in 1844, wrote:

There are, however, if I understand Mr. Sedgwick and Mr. Murchison, rocks stilts
lower; those which are now considered by them as metamorphic. They are the —

Cambrian of Sedgwick, and not the Upper, which latter I proved to belong to the ox
New York system. That the Taconic slate is precisely that in which the Nereites in 7
Wales occur, there is not the slightest doubt in my own mind, and this is that part of | ;
_the Taconic system which we can see-lying unconformably beneath the oldest mem-
ber of the New York system, and hence of the Silurian also. I know not, however, —
whether in Wales the same limestones, slates, and quartz rocks are to be found which —
we have here, and which are the oldest parts of the Taconic system. These are facts —
to be determined. Their non-existence in Wales, however, does not destroy the sys

tem. Very important members are known there, and should the lower slates a1 d-
**

al

well known here in New York, Massachusetts, Vermont, and Maine, and I may add; i
Michigan also.? Ry.

Under the influence of the publications of Sir R. I. Murchison, Amen
ican geologists, other than Drs. Troost and Emmons and the latter’s fol-
lowers, classified all the Lower Paleozoic rocks under Lower Silurian,

Lower Silurian. In 1872, however, Dr. T.S. Hunt published his history —
of the names Cambrian and Silurian in geology, advocating the recom
nition of the term “‘ Cambrian.?’? . nee ee

aoe

“39

1Sixth annual report of the geological survey of Tennessee by the State geologiat. "Nashville, 184, B,
p. 171, doc. ed., p. 4 of special ed. 4 <?

2The Talonic System, 1844, p. v. ; : ee 2

8Canadian Naturalist, new ser., vol. 6, 1872, pp. 281-312, 417-448._ Geological Magazine, im 10, PP a
385-395, 453-461, 504-510, 561-566, 1873. a

a ‘
‘

Mad oats A Ws =
: ee a "NOMENCLATURE —cAMDEIAN, . 241

lan im hed or Primordial will remain for those great and ha Soreaai fossiliferous
sits extending downward from the Potsdam in America and the Tremadoc in
; os and constituting an imperishable monument to the labors of Sedgwick and

3 A notice of the proposed change from “ Potsdam or Primordial” of
e first edition of Dana’s Manual of Geology to “ Primordial or Cam-
bri ran” in the second Jpenate was eee! in 1874;? and the term was

tie ch Parallel Surveys and in the U. S. Geological Baad in 1882.
Vith the exception of a few that prefer to use Taconic, the term is gen-
oral lly employed by geologists of all countries.

M ‘ost of ine neuen geologists of the present time draw the line be-

he ar the eis Rarsiadisiie From a study of the list of genera and
species of the fauna of the Lower and Upper Tremadoc slates, I. think
t the line of demarkation between the two systems would naturally
| between these two erento of the. Tremadoe. The fauna of the |

umbrian fauna, and there are sais a ioe genera cauit species more char-
AC teristic of the Silurian. The large fauna of the Upper Tremadoe slate
* characteristic of the Lower Silurian and the presence of a few genera
and species of essentially Cambrian type are not sufficient to include it
| the Cambrian. The fact that there is a slight unconformity at the
summit of the Tremadoc and the base of the Arenig is not of sufficient
‘al importance to warrant the placing of the line of demarkation

4 [ " a table showing the classification of the British sedimentary rocks,
pe Pret. A. J. Jukes Brown,’ the Tremadoc slates are placed in a stage
between the Cambrian and Ordovician.

Bt

This view of the Tremadoc slates was held by Mr. J. W. Salter,‘ who

ut a few words must be said about this band of slate, which so intimately con-

in fossil charactors from either.

Da af Nat., new ser., vol. 7, 1873, p. 1

1a, J. De Reasons for some of the changes in the subdivisions of geological time in the new
f Dana’s Manual of Geology. Am. Jour. Sci., 3d ser., vol. 8, 1874, p. 213.

1@ classification of stratified rocks. Geol. Mag., new ser., dec. 111, vol. 2, 1885, p. 297.

moirs of the Geological Surveys of Great Britain. Geology of North Wales, second edition,

ime

the Lingula flags below with the rocks above, and which is nevertheless so dis- —

=

vox oe Sa ONS ROS ots Oates Br tt eta Fg SBS eee ee

) A GRRE ae Le ae Lets? i eos Nat fae rai, ? Dh tebe ee

f Sef i oy e pat tee ee) yeas ‘s pe “ay
242 Pe eae tne Sa THE CAMBRIAN. Bis ea ai |

Dr. Henry Hicks! says of it:

:

+s The Tremadoc group, therefore, may be said throngk many of its types of fouled to
- link the Cambrian and the overlying Ordovician (Lower Silurian) formations t -
- gether, while it yet marks very distinctly the horizon in which all the ingly chara c-
teristic types in the Primordial faunas are lost.

- TACONIC.

- -The first proposition to apply the name Taconic to a system or seri aS
_of rocks is found in a gazetteer of the State of New York, published in
18422 The article is unsigned, but it bears internal evidence of having

been written by Dr. Ebenezer Emmons as his first presentation of the

views which were more fully elaborated and published later in the same

year. He describes the Taghkanic range, and states that the rocks
- composing the same are situated between the gneiss of Hoosie Moun ‘
Er tain on the east and the slates of the transition on the west ; that they
S bear a very close resemblance to the primary on the east, ane on the
‘other hand, a great similarity to the transition slates on the Wester ae
He says: k

It is not proposed in this plan to separate these rocks from the primary, but to
~ consider them as belonging to the upper portion and to speak of them as the Tag hs
kanic rocks, or perhaps as the Taghkanic system. * * * Considering them for the
present as belonging to the upper portion of the primary, the Taghkanic rocks wil

be composed, first, of a peculiar talcose slate, or a magnesian slate in part 5 in

other parts it is plumbaginous, which strongly soils the fingers. * * * Second, of L

- white, gray, and clouded limestone varying in texture from fine to coarse granular,
often interlaminated with slate, the wrigin often merely coloring the limestone so as

~ toimpart the clouded appearance. * * * Third, of granular quartz, ora sandsto ne
generally siliceous and of a brown color.‘ . a

_ In the concluding remarks on the Taghkanic avabeuk we read : a ; 4

On the whole, in regard to those rocks we have denominated ‘‘Taghkanie,” we de-
lieve they ought to be Bo whe a from ‘those on the east, being, as a se ne clear
distinct from them.®

A second memoir appeared in 1842, in which the term “Taghkanie” Wis is
changed to Taconic, and a detailed aan tie given of the geographic
distribution and character of the rocks forming the Taconic system.
A typical section is presented with the following comment:® —

The following section, extending from Petersburgh, Rensselaer County, to dams,

-

Massachusetts, embraces all the rocks in this system. Its direction is nearly ea aS

St

and west, or perpendicular to the strike of the system over which it passes. e i

10n some recent researches among Lower Paleozoic rocks in the British Islands. Proc. of t] the
Geologists’ Association, vol. 7, p. 9.

_ 2Topography, geology, and mineral resources of the State of New York. Gazetteer of the State o of of

New York, by James Disturnell. Albany, 1842, pp. 5-25. P

F

3Op. cit., p. 11. a ae
- 4 Op. eit., p. 11. : 7 seg ea
r 5 Op. cit., p. 12. .
, 6 Geology of New York, part 2, De ig the 7 of the 2d geological (northern) district, 1 2,
| *p. 145, Oy ae

nde the Taconic system west of the soaiubee ae end of the

¥ : TACONIAN.

This name was penposed by Dr. T. S. Hunt, in 1877, to include the
iy Taconic of Dr. Emmons,’ or the @ishular Quartz, Berkshire
limestone, and Taconic slates of the latter’s typical Taconic section of
S i842. At the time of the proposal of the name the author was uncer-
ain whether the strata included under it should be referred to the basa]
be ds of the Cambrian or to a pre Cambrian system of rocks.

| * b pre- -Cambrian horizon as compared with the Cambrian rocks from
hatregion. This is stated by himas follows: “This Appalachian Cam-

an series is wholly uncrystalline, and is separated from the Taconian
a

ides ape _3eepae period.”* As ue now anew that the Sieger

= base by an Upper Cambrian ‘adhd: and Tee original Taconic slate

0 pete Lower ‘Taconic “2 Dr. Emmons is ite by nA stratigraphic

PRIMORDIAL.

- This name was used by M. J. Barrande to designate the First fauna,
in ¥ : ontradistinction to the Second and Third.’

- The name was applied at first to the fauna, but, in 1854, in the first
tion of “ Siluria,” Sir Roderick Murchison designated thie formation
c ontaining the Primordial fauna as the Primordial Silurian, dividing

oA

th e Silurian into the Upper Silurian, the Lower Silurian, and the
E Primordial Silurian. The useof the latter term has been advocated more
0) less by those who oppose the use of the term Cambrian; but the
ne Primordial is now rarely used except when seddiisantia the First
ina of Barrande. -

the Taconic System; based on observations in New York, Massachusetts, Vermont, and Rhode
md. Albany, 1844, pp. i-vii, 67.

Emmons, Ebenezer. American Geology, containing a full statement of the principles of the
e, with full illustrations of the characteristic American fossils, Albany, 1856, vol. 1, pt2, pp. 49-66.
© geology of the Eozoic rocks of North America. (Abstract). Boston Soc. Nat. Hist., vol. 19

u 1, T. Sterry.- The Taconic Question in Geology. Mineral Physiology and Physiography. A
d series of chemical and geological essays. With general introduction. 1886, p. 677,

6 Bene ° Silurion du centre de la Bohéme, vol. 1, 1852, p. 88,
Ag

at ae

by a rea SM SES Oi A De Pi ORE SP yea ge eee
hi be 4 | ee ev | Yea sie © x Hi: is ata? e | S
3s NOMENCLATURE—PRIMORDIAL, vite 243

n a later paper he refers the Taconian system of the Appalachians |

by a stratigraphical break, and by a great interval of time, which in-

44 a separate Shomdir? was published i in which a a addition,

\

>

~

Ne ) Box A : . ms Pees ago Pe we wih t% hn Se
[RRL SEI BS THE CAMBRIAN. = Py a eed

- mons. In describing this sandstone, Dr. Emmons says: !

_ strata; and in no part of the county is there any rock which interposes itself between

_ always holds the relation of an inferior rock. * * * a

’ the reader. This rock at Keeseville has been rent in the most remarkable manner; a

~

-vania, Virginia, North Carolina, Tennessee, and Alabama; westward ty

- border of Lake Ontario will be a matter of some difficulty. It is geologically belo

426 nidhes oe Pre we z 2} ~ eel me I eee ee
Mik ee Pte, Se Re aS gee ee TT ASA ee oe ee
‘ =f eS -. of F = “wee ay *,

’ <2 & >» =,

Pt pe hela | POTSDAM. BY a 5 ak a

There are several early references to a sandstone oaeurnned at ‘the he
base of the section in the Upper Mississippi Valley and about the Adi-
rondack Mountains in New York; but it was not until 1838 that it was
well defined and given a distinct pans This was done by Dr. E. Kir n-

a,
I shall not enter upon its geological relations any farther than to state that, j nD
‘Potsdam and other towns in which it appears, it uniformly rests on the primary

it and the primary, so that is appears here as the oldest representative of the transi-
tion series. The identification of this rock with the sandstones along the southern

the transition limestone, and never in the northern district alternates with it, but

This rock is a true sandstone, of a red, yellowish red, gray, and grayish white colors.
Ttis made up of grains of sand, and held together without acement. Intermixed wit h-
the silicecus grains are finer particles of yellowish feldspar, which do not essentially
change the character of the sandstone, but they show the probable source from which |
the materials forming it were originally derived, viz, some of the varieties: of granite,

On the Lake Champlain side of the Adirondacks it is described as
follows: Ph? 2 a

Its position is evidently beneath the transition limestone and oalolfecosis sundneel ce
It is very deficient in organic relics, though not entirely destitute of them. It is
unnecessary to repeat what has already been said of this rock; it is purely qaartiaal
or siliceous in its composition and finely stratified. It dips to the northeast at Port t
Kent at an angle varying from 5° to 10°. The places where it occurs along Lak e
Champlain are indicated on a map of a part of this [Clinton County ], to which Irefer

several fissures, the principal one of which extends nearly a mile, and through whieh he %
the Au Sable flows, have been opened by some convulsion in nature to the depth, i
some places, of a hundred feet and from five to twenty wide. Near the bottom of ted
fissure at High Bridge, as it is called, I discovered numerous specimens of a small —
bivalve molusca, a lingula. I found, also, on examination, that the same fossi
occurred throagh an extent of 70 feet at least, and so far as I could discover, it wa:
the only fossil inclosed in the rock. It is extremely thin and delicate, yet the shell
is perfectly preserved, and is probably one of the oldest inhabitants of the globe, as.
the rock in which they occur is the oldest of the transition series.? © ; a

The name “Potsdam sandstone” was quickly accepted by the New
York State geologists, incorporated in their annual reports, and used in —
the final report on the geology of the State. The extension, by corre-
lation, of the name to the Southern Appalachians, through Pennsyl-

through the Mississippi Valley and the Rocky Mountains, and north
into Canada, and down the St. Lawrence Valley, rapidly followed, until
the name Potsdam is now used to typify the Upper Cambrian sone in
all parts of America. ee ke

=

~1 Report of the geologist of the 2G geological district of New York. earn annual report of the Geo
togical Survey of N. Y. Albany, 1838, pp. 214, 215, : c :
#Op. cit., p. 230, a, Siang” =s “i ie

- me ort s: of -
fms fea" a cites a a ps: Ex Ans i fo,
Be NeS c 0 eS mar ict !
eee NOMENCLATURE. eos (E

~

ee sie Se ST. CROIX.

ame ‘St. Oroix was proposed by Prof N. H. Winchell in 1873
| f 3 fossiliferous sandstone beneath the Lower Magnesian limestone

t he ¢ Mississippi Valley. The reason given is that the sandstone iden-
, Me by Dr. D. D. Owen as the Potsdam sandstone is unconformably
pel rjacent toa series of quartzites in Wisconsin and Minnesota that
he true equivalents of the Potsdam sandstone of New York.!

presence of the same fauna in the typical Potsdam sandstone on
northern side of the Adirondack Mountains as that found in the
Ip) ar sandstone of St. Croix Falls negatives this view and correlates
h ne sandstones that are unconformably superjacent to the lower quartz-
s with the typical Potsdam, and refers the lower quartzites to the
( bakian. The name St. Croix, however, is retained for the fossiliferous
mbrian sandstones of the upper Mississippi bia cul in Wisconsin,
a and Minnesota.

MADISON.

The > name Madison sandstone was proposed by Prof. R."D. Irving,?in
, for a band of sandstone consisting, in large part, of nearly pure
8 quartz sand, with a thickness of 35 to 50 feet, and lying between
i base of the Magnesian limestone of the Lower Silurian (Ordovician)

MENDOTA.

‘This name was proposed by Prof. R. D. Irving, in 1877, for a cal-
Cé careous § stratum near the upper portion of the ‘*‘ Potsdam” formation of
Wisconsin. It is formed of alternating sandy and calcareous material
th a » iD the upper portion, is almost a well marked and very persistent

TONTO.

| ea of Fae Colorado River, Arizona. He considered the formation
f Primordial age, and it has since been found to contain an Upper

brian fauna. — It was more fully described by him in the following

meral sketch of the geology of Minnesota. Geol. and Nat. Hist. Survey, Minnesota, Ist Ann.

Rep. for 1872, 1873, pp. 70-72. ;

cs Che Lower Silurian rocks. (Geology of central Wisconsin.) Geol. Wisconsin, survey of 1873-1879,
2, 1877, p. 525.

vane bid., 525. :

40 eles of the Tonto sandstone. (Abstract.) Washington Phil. Soc. Bull., vol. 1, 1874, p. 109,

4 o> plorations and surveys west of the 100th Merid., vol. 3, 1875, p. 163; pp. 521-522,

dans beatin a ee eee Boge Rn ORR a eR eee Se

“F P Oy abe Je ae yee oe 2s RU AA eke
* K - a. a Bk thse? ¢ or a a ey tay “2 ‘ ss 2 eee
ie a hee Seek Ca — Tea Oke ys ae i a a ae oR pees dag’ see. <
ye A . ‘ . = ey a rd, : ant <a ~ . ‘ we
a 246 Ligh Set seen eee | THE CAMBRIAN, Paap Sn es youn. 81
7% - @ hh \ 7 % 7 % ’ ‘ ee ia a > e: ye “lo
Beara e Ci) “HAMBURG. Ap SAO aa
sa

he ‘ : SO
The Hamburg limestone and the Hamburg shale are names ‘used | y
Mr. Arnold Hague, in 1881, to designate the Upper Cambrian limestone e
and shale of the Cambrian section of the Eureka district, Nevada. Th 1e
limestone is superjacent to the Secret Cation shale and subjacent 1 to
the Hamburg shale. The latter is characterized by a well develo
Upper Cambrian fauna.

Ss
-

SECRET CANON.

ee This name was applied by Mr. Arnold Hague, in 1881, to a bande of ¢
oe shale in the Cambrian section of the Eureka district, superjacent to the
Ar Prospect Mountain limestone and subjacent to the Hanbun limestone, i
. - characterized by a fauna that may be referred to the upper portion « of
the Middle Cambrian.? Sa
KATEMCY. - Rt oot oy

Prof. Theodore B. Comstock, in describing the Upper Cambrian. rock
of the central area of Texas, proposed the name “ Katemey” for t the
‘“‘ Potsdam series,” or Upper Cambrian.(?)> This terrane is named from
the beds exposed in the valley of Katemcy Creek, Mason County.

> . “~ - / ~~

RILEY.

This name was proposed by Prof. Theodore B. Odwntock, for a seri
'_ of sandstones which he considered to be superjacent to the Hickory ry
mi, series of the Central Texas, Cambrian section, and subjacent to the
ei Katemey or Potsdam series. He referred it provisionally to the Mide dle
4. Cambrian zone.‘

a . HICKORY.

Rest This name was proposed by Prof. Theodore B. Comstock, for a seri S
ae of strata that he considered to underlie the typical Potsdam Sandstone
_ of the central Texas section. He referred the series : provisionally to
the Lower Cambrian.® . ae
we . CONNASAUGA, —_ ye, a
This name was proposed by Mr. ©, Willard Hayes, for the Cambria 0
wee shales at the summit of the Cambrian section in northwestern Georg al.
He correlated it with the Knox shale of Safford’s Tennessee section,
ea assigning to it a thickness-of 1,600 to 2,000 feet.® |

x . oh eS MS WROTE TE ES Vo, OT ER BOK PE AT !

mre

- . * - ' Report (on work in Eureka District). U. S. Geol. Sury., 2d Ann. Rep., 1880-81, 1881, P. 27; 3a Ann n
Rep., 1883, p. 255.

ae

: ‘re 2Tbid., pp. 27, 253. 4 oe i x
a ’Comstock, T. B.: A preliminary report on the geology. of the central ‘mineral region of * exa
mk First Aun. Rept. Geol. Surv. Texas, 1289, p. 289. = * $

‘ 4[bid., p. 286. iE ' ——
fis 6 Ibid., p. 285. : eo
6 The overthrust faults of the southern .Appalachians, Bull. Geol. Soe. America vol, 2, , Feb. 18 39 1,p
: 143, pl. 3. ; Y cptiame ee

x > 4 >> :
o— yaw - a
: >.

~ é ; 2 ‘ t. Ne Sal

sb ig cane Se aR cael i ais een
aie eS sie a sae Ee am NOMENCLATURE. 3 : i we oe
* by ie *. ?

o gS eee sé

-_-

This 1 ame seems ms to be a synonym of Montevallo Shales proposed by —
-rof Eugene A. Smith.
a Apts. am. x ’ - > _ :
Ly wae ee! = >. P : =
‘aa x ewe MONTEVALLO. |

, cr
a,

» name Montevallo, or Choccolocco, shales was proposed by Prof.
gene Srhith, for a series of sandy shales of a great variety of colors,
ie ch as olive, green, brown, chocolate, yellowish, etc., that occur above
]
voosa shales in northeastern Alabama.!

By 3 name appears to be equivalent to Connasauga shales mh saan
b Mr. ©. Willard Hayes.

aa
ae CHOCCOLOGCO.

isis apparently a synomyih of Montevallo.

ss i. : ian
"US COOSA.

_—_—

=
TL,

The name Coosa shales was proposed by Prof. Eugene A. Smith for —

ihiaies in the Coosa Valley at the base of the Cambrian section.
r Th ey a ae described as thin-bedded limestones with clay seams be-
U tween.

fore the Geological Society of America, December 29, 1890, and pub-
li shed February 9,1891. It was applied to the series of piaiee: some
3,000 feet in thickness, occurring at the base of the Cambrian section

in northwestern Georgia.’
if + : =
Pe 4 ae ROME SANDSTONE.

Se

- This name was proposed by Mr. C. Willard Hayes for a sandstone of
Cambrian age occurring at Rome, Georgia. In connection with the

Weisner quartzite it is given a thickness of from 2,000 to 3,500 feet.
‘he correlation is with the Knox sandstones of Tennessee.‘

‘ *
—
co)

ais . BRETONIAN.

rs ees name is applied by Mr. G. F. Matthew to the upper series of
0 brian rocks as found in the vicinity of St. John, New Brunswick,
id on the island of Cape Breton, where the fauna of the division is
we All zeeetopet: It will be arranged as an Upper Cambrian forma-

_ Geological structure and description of the valley region adjacent to the Cahaba Coal Field. Geol.
§ 2 egg Report on the Cahaba Coal Field, pt. 11, 1890, p.148, (Issued January, 1891. )
1.,p. 148. — :

STI 1 overthrast faults of the Southern Appalacians. Bull. Geol. Soc. America, vol. 2, Feb., 1891,

wae

+P, 143.

as
:

“This name is 4 used by Mr. C. Willard Hayes in a paper read be-

- Cambrian section. This includes the fauna of oie Paradoxides zones 3

Prof. Jukes to the slate series of St. John’s, described as from 2,000

_ Adv. Sci., vol. 16, 1867, pp. 117-119. ae

tia, New Brunswick, and Prince Edward Islands. 2d ed., London, 1868, p. 638.-

i 2 kann eae tse THE CAMBRIAN,

of America it may be recognized.’

subsequently found trilobites of the genus Paradoxides in the slates’ ty) a

— /p.- 129.

ReMi tn Seamer aba eS MLE A

a ed a sth *

~ Pas
“ Pad

SAR Seo) nt ioe a pee iS Ze,

‘The name Acadian was proposed by Sir J. Ww. tabs in 1867
the series of rocks represented in New Brunswick by the St. John slate
of Mr. G. F. Matthew.1| In 1868 these observations were i R
with the statement that the discovery adds a new formation to the P
leozoic period in America. Hesays: - : ee ae

This formation has as yet been known as the “St. John zromp,? but I think thi is
name unsuitable, both on account of the number of places known as St. John and on E
account of the variety of formations occurring near St. John, in New Brunswick, au id
would propose for the group now under consideration, hiaveekottied by Paradoxide

Conocep halites, etc., and the oldest known member of the Paleozoic of America, the :
name Acadian ated by which I hope it will be known to geologists in whatever part

_In-a recent paper on the fauna of the St. John group, Mr. G. F. Mat. b-
thew limits the term Acadian to his Division 1 of the New Brunswick <i

ST. JOHN'S. ie 3 ;

Prof. J. Beete Jukes in 1843* used the name St. John’s slate for the

slate as seen near St. John’s, Newfoundland, beneath the Signal Hill :
sandstone. When referring, in 1862, to this work he states he did not

find any fossils in the lower slate formation, but that. Mr. C. Bennett,

the west side of St. Mary’s Bay. These were named P. bennetti by } fr.
J. W. Salter. On the map accompanying the report of 1843, the slates”
of St. John’s extend southward from St. John’s and around the souther n
point of the Avalon Peninsula.to and about the Bay of St. Mary’s. ES e ss
The investigation of Dr. Alexander Murray and Mr. J. P. Howley in
connection with the geological survey of Newtoundland, have show
that the slate carrying Paradoxides about St. Mary’s Ray is a later
formation than the slate at St. John’s; and that the Paradoxides. slate s
are unconformably superjacent to the slates to which Prof. Jukes gave
the name of St. John’s in 1843, This restricts the name as given b by
to 3,000 feet thick. It was in this series of slates that the Rev.
mises Harvey discovered the fossil which Mr. Billings described as |
Aspidella terranovica. The entire series, along with the Signal Hill.
sandstone of Prof. Jukes, was referred to the intermediate or Huronian
1Qn recent geological discoveries in the Acadian provinces of British America. Proc. Am. As $00.

-* Acadian geology. The geological structure, organic remains, and mineral resources of Nova co =

’Iluscrations of the fauna of the St.John Group No. 5. Trans. Roy. Soc. of ‘Canada, vol. 8, ton,

4General report of the geological survey of Newfoundland in 1839 “a 1840. erie 1843, p. 59, 24 yy
5 The Student’s Manual of Geology. 2d edition, Edinburgh, 1862, P- 457. as

y Dr. Murray ; he in the classification used in this memoir
ac) saded under the Algonkian, as a pre-Cambrian formation. _

proposing a classification for the formations in the vicinity of St.
n, New Brunswick, Mr. F.G. Matthew proposed the term, “St. John
1p” for several zones of soft black and dark gray, finely laminated

srous thin beds of fine-grained sandstone.’ The fossils were Lingula, a
yn hifer, Annelids, and Coprolites. This was republished in 1865, and
ii use in all the latest publications by Mr. Matthew.

x oe n view of the fact that the term “St. John’s” was used for a distinct
f mation by Prof. if ukes in S iivets u appears best to continue to apply

ae JOHANNIAN.
ey ots

_ This name is proposed by Mr. G. F. Matthew for a local series of
strata in the St. John basin of New Brunswick that occur between the
Paradoxides zone, or Division No. 1, and the Upper Cambrian ria or
z divis sion No. 3, which he calls Bretonian.?

GEORGIA.

Tro ing slate belt of Rutland County, Vermont, that passes into Wash-
ing on County, New York. A provisional reference was made of a
ries of clay slates that occur in the central part of the State.t A full
scription of the formations referred to the group is given in the text,
ne their geographic Seng oation is delineated on an accompanying
j LD. . f
Prof. Jules Marcou advanced the claim that he first used the name
Geo gia in October, 1860, which was followed in December, 1861, with
a a full definition of the group.’ Prof. Hitchcock in reply to this, seated

0] fatthew, G.F.: Observations on the geology of St.John County, New Brunswick. Canadian
B Wat. vol 8, 1863, p. 244.
eeeyeisetioas of the fauna of the St. John Group No.5. Trans. Roy. Soc. of Canada, vol. 8, 1891,

4 2On the Primordial Fauna and the Taconic System, by Joachim Barrande, with additional notes by
iles Marcou, ‘Proc. Boston Soc. Nat. Hist., vol. 7, 1860, p. 375.

AR chcock,C.H. Geology of Vermont, vol. 1, p. 357.

5 “6The Taconic of Georgia and the Report on the Geology of Vermont. Memoirs Boston Soc. Nat.
‘His t., vol. 4, 1888, pp. 123, 124.

~ >

~ -

+7 As ae es ae ET ee ey * Front! x

ik gees rr nes ae Sad te Ce Bie ig, oh oe a
Phy AY td

Reaves eS. | NOMENCLATURE. pet tae

les alternating with zones of coarser grained slates, containing nu-—

wn of Georgia, Vermont. There was also included in the group the —

Ag
.

| that paral from Polame 1 oft the Bones of venti were. 0 distefb t
prior to December, 1861, and that it was in print by J uly, 1861.1 byt

. ; published i in 1865, the Georgia group of Prof. Hitchcock is included.
with the “ Red Sandrock” in a common color, and is so referred to ins

gia series of Prof. C. H. Hitchcock as one formation under the name

with the oe of the Georgia series, in the Middle Cambrian or Geor-
gia group.” The reference to the Middle Cam brian was changed to
Lower Cambrian three years later.’ } ce

“was accepted by Dr. KE. Emmons? in 1842 and placed as the second —

- limestone and: the third bed of limestone. This section was corrected 4

as expressed in the nomenvlature of the New York aaah the Red

‘of Vermont, and the name Red Sandrock was applied to the latter,

k
x
ot ’

On a map, in the afin accompanying the Geology of Canada for 1863, |

the legend. This includes the ‘‘ Red Sandrock” series and the Geor.

of Potsdam.
In 1886 the “Red Sandrock” was included by Mr. 0. dD. Walcott.

-

GRANULAR QUARTZ.

This is one of the first formations differentiated and named by Prof. F
Amos Eaton.‘ He referred it to the Primitive class and indicated its
stratigraphic position on a section accompanying the index. The name

member of his Taconic system, between the second bed of Stockbridge a

in 1844, so as to place the “ Granular Quartz” at the base. of the Taner :
system.® ;

In 1887 the Olenellus fauna was discovered by Mr. C. D. “Waleott i in
the “ Granular Quartz” near Bennington, Vermont, thus dctenaiiinan
its pre-Potsdam age,’ . aa

RED SANDRUCK, _

The occurrence of a red sandstone at Burlington Falls, Vermont, was
mentioned by Prof. C. T. Jackson in 1844.8
In the scheme of Dr. C. B. Adams, illustrating the rock 8 of Vermeil 7

Sandrock occurs above the Hudson River shales.?
The correlation thus indicated is that of the reddish brown Medina ee
sandstone of the New York series with the reddish colored “sandstone”

thus: originating a term that has continued in geologic literature, not-

1Date of the publication of the report upon the ( Geology of Vermont. Boston Soc. Nat. Hist. Proe.,
vol. 24, 1888, p. 34.
_2U.58. Geol. Survey, Bull. No. 30, 1886, p. 44.
3 Stratigraphic position of the Olenellus Fauna in North America Send Europe. Am.Jour. cg a
ser., Vol. 37, 1889, p. 383. 4
4 An index to the Geology of the Northern States, with a transverse section from Catskill Moun ain

tothe Atlantic. Leicester, 1818, p. 21. - =

5 Geol. of N. Y., Part 2, comprising the survey of the 2d Geol. (Northern) District, 1842, p. 144,
6 The Taconic System; based on observations in New York, Massachusetts, Vermont and Rhode
and. Albany, 1844, p. 18. :
7 Discovery of fossils in the Lower Taconic of Emmons. Am. Assoc. Proc., vol. 36, 1888, p. 213,’ 4

6 Final report on the Geology and Mineralogy of the State of New Hampshire, 1844, P- 161,
® First Aun, Rep. on the Geology of Vermont. Burlington, 1845, p.61, —

vi eugd tho fact that the rock itself is a magnesian limestone

tie = of a section of Snake Mountain, Addison County, the strata cap-
ping the: mmonptains are designated. ae the name of Red Sandrock.! -

-

3 : weg PRIMAL.
de lefined as follows:

ve

‘The equivalent expression was Formation No. 1, and both terms have
been used in the geologic work of eitnrad insite Maryland, and Vir-
ginia, but they have not come into ponpral. use.

CHILHOWEE.

, a series of sandstones and shales superjacent to the Ocoee conglom-
. erates and shales and subjacent to the Magnesian limestone and Shale

inestone.®

q “quartzite of Chilhowee Mountain, the Chilhowee Mountain quartzite is
re erred to the Lower Cambrian and correlated with the Granular
qu nartzite upon the western slope of the Green Mountains of Vermont.

WEISNER.

fae of quartzite that oceur in the Montevallo shale of nore

: lartzite of, Tennessee. This correlation is probably incorrect, as the
‘ati tter quartzite is of Lower Cambrian age.*

a This name is also used by Mr. C. Willard Hayes for a series of quartz-

ites that occur between the Coosa shales and the Connasauga shales

| the Cambrian section of northwestern Georgia. ‘In connection with

dstone, Potsdam or Chilhowee, Prof. Safford’s eee section,

Profs. Smith and Safford.

cond Ann. Rep. of Geol. Surv. of Vermont, 1846, p. 163.

Sei ool 47, 1844, p. 155.
we A geological reconnaissance of Tennessee ; first biennial report. Nashville, 1856, p. 152,

a Rept. on the Cahaba Coal Field. . Pt. 11, 1890, p. 149.

a eat cs ue he t, rn ue pen ee Ay Tw Sry aby eee pe ve a " he
wis se. a os ep hte 2 tas = hi
> : 3% : < pO ae oy oy i = '
+ SSE Ae a aa MENCL E. 251
te _ NOMENC ATUR
nd oo 4 ; /

i In the Heeond annual report of Vermont by Dr. Adams, in the descrip- —

z “The term Primal was proposed by the brothers Rogers . in 1844 4 and

The: name Chilhowee was proposed by Prof. J. M. Safford in 1856 for.

| gl group, or what was subsequently called the Knox shale and the Knox»

a "By the discovery of the Olenellus fauna in the shale resting upon the

abama. He correlates’ the quartzite with the Chilhowee Mountain

Rome sandstone he mentions the correlation of it with the Knox

awe faults of tie southern Appalachians. Bull. Geol, Soc. America, vol. 2, Feb., 1891,

SS Our Primal series cmiradcs the four great rocks between the occ of the Paleozoic —
ER and the base of the first limestone, the Calciferous sandstone of New York.2

:

ES Sts se PN os Beis Petes ee ee aoe :

ae roe A ae CAMBRIAN, Pause
eee = mete es % = ¥
ee This name was Sc by Prof. J. M. Safford i in 1856 a a ‘series 0 of
we “hi conglomerates and slates that he considered to be superjacent. to the |

ia ae group and SPEme to the Chilhowee SAREE.
; PROSPECT.

eet For the Seats members of the Cambrian section, in the Eureka dis. ;
triet, Nevada, Mr. Arnold Hague proposed, in 1881, Prospect Mountain —
quartzite and Prospect Mountain limestone? As now known the up- —
per portion of the Prospect Mountain quartzite is characterized by the ©
~ Olenellus or Lower Cambrian fauna, and the Prospect Mountain lime. ;
stone by the Middle Cambrian fauna of the Rocky Mountain section.

EASTERN AND WESTERN SANDSTONE,

These names were applied to the horizontal, evenly -bedded sand
stones of the south shore of Lake Superior, east st west of Keweenaw —
Point, by Dr. R. D. Irving in 1883 as convenient terms under which to

describe the character of the sandstone and aa geogrephie: distribu.
: tion.® .
: LAKE SUPERIOR SANDSTONE.

ae te-. Dr. J. J. Bigsby described the red and white sandstone sine th
es south shore of Lake Superior as early as 1825, and in the account | 0 ‘
the geology of Lake Superior by Capt. H. W. Bayfield, he speaks of
the sandstones of Lake Superior.4 As used by Capt. Bayfield, the Lake
Superior sandstone included both the Cambrian sandstones of the south
--. ghore, and the pre-Cambrian sandstones of Keweenaw Point and the.
north shore of the Lake. It has been used by various authors in the
same general manner, and has little value as a term in stratigraphic 7

Aa ~ geology. He | | Pare
ee ' POTSDAMIC. — Oe oe eee

i=

soe é rs >
cc ae 5
4 aks

ss» Prof. C. H. Hitchcock proposed in 1888 for ae rocks® coptaining the

Sets ee ‘ ae

Cambrian fauna, the name Potsdamic or Taconic.

. — re ee eee ee ee eee hws re

pet a 3 1A geological reconnaissance of Tennessee ; first biennial report. Nashville, 1856, p. 151. >
F 2U.S. Geol. Survey, Second Ann. Rep., 1880- 81, 1882, p. 27; 3d Ann. Rep., p. 254. ‘ :

a ke - §The copper-bearing rocks of Lake Superior. U.S. Geol. Survey, Monograph, vol. 5; 1883, pp. 351, 3 65.

a 4 Outlines of the Geology of Lake Superior. Quebec Lit. and Hist. Soc. Trans., vol. 1, 1829, pp. 15-22. —

3)
>

xs ed 6 Date of the publication of the report upon the Geology af Vermont. Boston Soc. et Hist. E 3
- vol. 24, 1888, p. 37.

ait < ES PST L ack Lys ae” SP Sut Sih ee Ses Sy edllet thet e ak oes Ben ete Sy cbr.” F)
4 sone % ike 4 ae “ers . a 4 < m4 oe
ee & ? “d cA a ai - ee « = v& s mn ee

. ; . + Bo Saree A Ee ie
ay war : sl 7 + ’ aed * <=. or al
= — t y ~ Se eh z=
rg oF ot ae bE a - ._
¥ a 4 > eX 2
=e $ M —- Ac
s “K , ay - re =
- ~ >

. CHAPTER | * Z

wT

MMARY OF THE PRESENT KNOWLEDGE OF THE FORMATIONS.

-

ie? The ‘data andor this heading is assembled for each of the following
a dlogic Provinces:
Atlantic Coast Province. . ;
; eee one Province. . “he
f Eeory Mountain Province. ae ae
ie Interior Continental Province. tape oe
os brief résumé is given at the end of the description of the forma-—
ti ae 1a each province and a general résumé of the Cambrian Group at.

ATLANTIC COAST oh echoes .

RPh Griisinies the rocks ripened: to the Cambrian group on the Island

eens and the adjoining coast of Labrador, the provinces—
| ova Scotia and New Brunswick, and Cape Breton, and the States
of N Maine, New Hampshire, and eastern Massachusetts.

NEWFOUNDLAND AND THE ADJOINING COAST OF LABRADOR.

] nd 1 is obtained Saree from the sabientidea of the Geological Bios
of “ag for the northwest and west coast and the Labrador coast,

€ Cambrian strata on the adjoining coast of Eabrador are included
_ those of the Cambrian area of north western Sie apneic as

aT LW. E.: Geological Survey of Canad Trepor’ of progress from its commencement to 1863.

SS en er ED Oe Oh ee ete se ee a ta: Ser eal = ;
1 3 a . : - A . =~ me NV ae a oe ae Gs wee > ae yy 5 d c 4 ; re a ma 4~ 7 Pe gh -. gare
‘ tee eh ‘ fa Ss ~~ they r.. Fane a ey bas % ary 4 i . i. <P>

_— ° yy Ae.

c my ‘ is ? eed ee Me : ae oe ich. +8, oe

ai % » th OA + fONB iota Bie: came ak ¥ Pe | “on el are ty

eee, arene tt Bi athe ae THE CAMBRIAN. ; Seeks [BUELL BL

a) . : | . is PVA Re Si eS
es hh nt &e

SY. 143 feet of gray, reddish and greenish limestones, The section is, n ‘
R Retat, as follows : | pres: BESS tO ea

Koay = F < >
*

oie . CS Say in Feet.
; 1. Red and gray sandstones, sometimes of a reddish gray; consisting, in the
lower part, of a conglomerate composed of rounded pebbles of white quartz
_ from an eighth of an inch to 3 inches in diameter, in a matrix of fine-grained —
¥ sandstone, made up of whitish and reddish quartz, and white and red feld- _
Y - ss spar. A similar fine-grained mixture constitutes the great mass of rockin
-. * the upper part. The beds vary in thickness from 3 inches to 3 feet, and many
Jeg of them are penetrated vertically by Scolithus linearis, about a quarter of an
Sas Sere: inch in diameter, and always of a lighter color than the surrounding mass.
—-—--- Four feet below the summit there is a bed 3} feet thick, of a mammillated or
Bao, concretionary character; the concretions, which are Sent 1 to 10 feet in hori- |
,—-- gontal diameter, being daiainedl of concentric TOES from a quarter to half Le
Se -emanenh thick 22.05 3 Lis bop deat coe lent nis main gl i alk oii hile ee 231
—Q. Gray, reddish, and greenish limestones, Desens on the strike great diver-- 4
sities of character. They sometimes consist of yellow-weathering, massive,
nodular, argillaceous limestones, probably magnesian, holding lonbiduie:
patches of pure limestone, as well as of red and green shale from 3 to6 —
feet in horizontal diameter. On the strike these yellow-weathering lime-
stones pass in some parts into gray, compact, pure limestone, in thick, .
eel 2: massive beds, while in others they are evenly divided into layers of only 2 |
ae or 3 inches thick. In Forteau Bay the whole mass appears to be moreor —
Berg legs. fosailiferons 2.5 Ja\5)- o> dwn arewe owe poninnn <gunic sae => csinate sen dom <oences Se

I examined the collections from these limestones now in the Canadian 4
o Geological Survey collections, and found the following species, most of e
which had been recognized and described by Mr. Billings: :

WS Palwophycus i incipiens. Stenotheca elongata.
“eee Archxocyathus profundus, | rugosa. :
MS ae _ Spirecyathes atlanticus. . Hyolithes billingsi. ea
a ‘ Coscinocyathus billingsi. . Salterella pulchella. Fo:
esea : Iphidea bella. | rugosa, :
oo Sagan _ Kutorgina cingulata. Olenellus thompsoni ?
Pic: labradorica. Ptychoparia miser,
- are Obolella chromatica. Protypus senectus,

a ; Orthis 2 sp. Solenopleura (like S.nana),

- In describin g the extension of the rocks along the north shore of the y
- Straits of Belle Isle, Sir William E. Logan states that they rest on the
Laurentian gneiss, and extend along the coast for nearly 80 miles, with 4
a probable breadth of 10 or 12 miles, and slope towards the water at an _
average of about 60 feet to the mile. In this stretch along the coast
they are divided into five or six tabular masses, separted from one ans
other by narrow denuded portions of the gneiss. al
S., On the Newfoundland shore sandstones occur that. were raltsed Wy
the Potsdam sandstone from their stratigraphic relations to superja-
cent limestones containing Lingulepis acuminata? The data, however, ©
does not fully sustain this reference. Following south along the west

ate > 1 Op. cit., p. 287. . ; * Op. cit, p. 289,

{ opie ead with that is described in detail, as follows :!

Ҥ y y ie ore. arises a range of hills of Laurentian gneiss, 2,000 or 3,000 feet i in height,
etiene of which i is exposed the follow ing measured section ;

ot ae rites A.

A ‘ ~ Feet.
Bacio blue, fine-grained slate, with a cleavage independent of the bed-

: ding. Of this slate only 105 feet of the upper part are seen; the lower
3 part is concealed in the space between the upper portion and the gneiss,
and may comprise a thickness of about 230 BO at yrs glans sas FP Ba 335
2 Blackish blue slate interstratified with gray quartzites, in beds of from 6 *
; inches to 3 and 4 feet. In the 80 feet at the bottom the quartzites

greatly predominate, and they constitute 15 feet at the top, while the in-.

eee : 605
ers at" 2 oe B.
1 Light gray, yellow- weathering limestone, in beds of from 1 to 3 inches thick,
_ interstratified with blackish-blue, slightly calcareous slate, both contain-

x ing small specks of silver-white mica, which are more abundant in the —
Vn limestone than in the slate. The limestones hold in abundance fragments
Beef trilobites, chiefly belonging to three or four species. Among them is
- Paradoxides ( Olenellus) vermontana, a new species of Bathyurus, and the>
pygidium of a species so closely resembling B. extans of the Birdseye and
_ Black River formation, that it can scarcely be distinguished from it and .
Be: SMITE We tle GAING 5022s sown vt ee nest toca eee ieece re reuse - 80
2. Grayish green, micaceo- -arenaceous sala, interstratified with a few beds of

Bt grayish quartzite weathering sli ghtly FOLIO Wire tc oeoas Hp da Statins ba wik don 80
3. St ae cried omnia ntaik' vain cb eke sad horn cede dhanascceasans 30
4. BR eddish granular quartzite in thick beds, with numerous parallel joints in
i>: two directions, dividing the beds into rhomboids...--.........-.. ---.-.-- . * 105
5, Gray and grayish green, micaceo-arenaceous shale in beds from a quarter of
an inch to an inch thick, interstratified with a few beds of gray, very fer-
pe: -ruginous, sandy dolomite, and fewer of gray quartzite......-....--.-.--. 127

Gray ‘arenaceous dolomite, weathering yellowish brown, interstratified with
” > reddish quartzite in beds of from 1 inch-to 1 foot thick, and with reddish
a and grayish micaceo-arenaccous shale predominating towatd the top. The
Bete of dolomite and shale contain fossils, among which are Obolella chro-
matica ?, Obolus-labradoricus, Parado.xides vermontana, Concephalites, a new

jpecies of Bathyurus, and one or more undetermined species of Salterella. 27
Ly 483
a ; C. ae
ae tl.
.W Vhitish quartzite in beds of from 6 inches to 2 feet, interstratified with
i ‘light gray, micaceo-arenaceous shale, in layers of from 6 inches to 1 foot,

yh lich occur at miervals of from 5 tp 10 feetisc.. so< sos e oc. Sek ne eee. 180

ss a ae to Eee “aie a more eeteddsa section of Cam-

Bee aivdiate 175 feet consist chiefly of slate........-...-2.---2-e--es ene 2 MeO
oe, 7 ad

3. Reddish quartzite, in beds of from 1 to2 feet thick .........-....-..+...-.-- 34

ae

<

-

/

—

e 6. Gray, pure limestone, composed of comminuted organic remains, belonging

, ‘ a 5 Ae 5AM pote
LER vty — ey as Shai. yeas con pia ees pe Ngee ao hore
- NF ma eae %P ors ae ube : s s, 2. ye Seine s ,
256 kd att ae THE ‘CAMBRIAN. - a Ok i ae Sane

designated as Potsdam that is continued aes into the valley of the

~ ¥ ; e

2. White and reddiah TA in 1 beds of from 1 to 3 feet thick, fatenabratiiegss 2
- toward the bottom witha gray arenaceous dolomite, weathering yellowish —

3. White and reddish ahavtatte 4 in beds of from 1 to 3 feet thick, interstratified —
with greenish micaceo-arenaceous shale, constituting about one-half the
MOMS on oc coe f.6 nae Sesh pec kg omah Meee els ghey ee eee ar bate ss ipen eee

4, Gray, pure limestone, in beds of from 1 to 3 feet thick, marked with a few

reticulating strings of yellowish-weathering dolomite. Therockisamass —
of comminuted organic remains, among which are Paradoxides vermontana,
and undetermined species of Bathyurus and Salterella, as before..-...-..

_ 5. Blackish blue, soft shale, interstratified with gray yellow-weathering lime-
stone, probably magnesian, in beds of 1 or 2 inches thick. The quantities
of shale and limestone are about equal, and the whole is intersected by
reticulating strings of cale-spar.... 1.222. 12-2 e228 cone cence ween bie oan ae

to Paradoxides, Bathyurus, and Salterella, as before-..........-.-....--. -
7. Bluish black, soft shale, interstratified with gray yellow-weathering dolo-
mitic bandsyas before: 3.56 3.22 3s se ccna nda ee vee set Le
8. Gray, pure limestone, probably composed of comminuted organic remains as ‘
before; underlaid by bluish black shale, inclosing nodules of blue com-
pact limestone, some of which weather yellowish-brown, and are prob-
ably magnesian i 22% 21 s0< Se sees Sa~Se wk kee Gide 1a Seas ee Cea oe eae
9. Bluish black, soft shale of the same character as before, interstratified with
afew beds-of quartsibe in si5 cass sen thbets aoe dene enan eee kpeeeie

etad -o.0) ae ee es Jiihn a al De ee 7

I examined the species of Bathyurus referred to in No. 1 of Division —
B, and also some other fossils labeled as coming from Bonne Bay, and
nee can be no doubt that some mistake was made in labeling the
specimens, for they certainly belong to the Trenton fauna and could
not have been assuciated with the Lower Cambrian fauna of the sec: x
tion. All the Paradoxides referred to belong to the genus Olenellus or
Mesonacis and several of the specimens of Bathyurus to the genus —
Protypus. If the section was correctly measured and the Cambrian —
fossils occur as mentioned all the strata belong to the Lower Cambrian, —
and the fauna is a part of the Georgian fauna of the Cambrian. From —
_the accessible data I am not able to discover that the Upper Cambrian —
or Potsdam fauna has been found on the northwest coast of Newfound-
land or on the Labrador shore. | Secs 2 ;

SOUTHWESTERN NEWFOUNDLAND.

On the *“* Map showing the distribution of the Silurian and Carbon:
-iferous Formations (ete.) in St. George’s and Port au Port Bays, New-
foundland,” by Dr. Alexander Murray, 1873~74, a considerable area is”

Humber. The reason given for the identification of the Potsdam Ter- 4
rane, in the Reports of the Geological Survey of Newfoundland for |
—1873~74, ’75, is that the strata placed within it are subjacent to the beds ~ e
containing fossils of the alciioroge formation of sv Lower. Silnriay 4 3

.
oo
8
ae
oa
es
ye

a Aine Ne
. 3
a> t
Ghtas
a
os

Me =
b
A
—
bS
|
=~]

not sufficient i in the absence of piper Cambrian fossils to estab-

ial sh 1 the presence of the Potsdam horizon on the southwestern side of
- Rg

he pis land.’ It is quite probable 1 that strata of Cambrian age occur, but
as yet st the proof of their presence is very defective.

? EASTERN AND SOUTHEASTERN NEWFOUNDLAND.

’ ~

“4
— *
rs

-. ) a!

he Che section at Canada Bay i is as follows, according to Dr. Alexander
ve urray : :

ES dionds Mountain bluish gray slates. conglomerates, and diorite.........-.. 2,500
B. § Salt Water Pond bluish gray, black, blue, reddish, and white limestones,
_ yellowish gray and black slates, and gray and white sandstones, in some
___ parts holding Olenellus vermontanus, Uingula, Scolithus and fucoids.._... 2, 000
Cig and dark blue limestones and brown slates, with cherty limestone at
_ the top ...--..----- Meech itl ewe sine aise Sine Ppa tends a cwed po kane a4 eee ae 900

—
~

| Sa e | 5,400 —
2 The strata referred to the Cambrian system in southeastern New-
endian’ are well exposed on the peninsula of Avalon and westward
long the coast to the northern shore of Fortune Bay, and northward, on
the western shores of Trinity Bay. Dr. Murray has given a Sonatas
Hecription of the terrane in the reports of the Geological Survey of
Bewfoundiand for 1868 and 1870; and a fine geological map ofthe
e eninsula of Avalon, by Dr. ices and Mr. James P. Howley, 1831,
s sh ws thedistribution of the Cambrian rocks. The correlated Section
is de ascribed as superjacent to pre-Cambrian ‘‘ Huronian” rocks and as
havi ving a thickness of nearly 6,000 feet, of which 138 feet are lime-
| stone e and the remaining portion arpillnebacs and arenaceous deposits.
ae ‘he section in gabe cag order is as follows :?
SS Feet.
(8) = and black micaceous shales, with gray micaceous sandstones of Bell
Island, Conception Bay. Organic contents are: two species of Lingula,
_ four species of Paleophycus, Hophyton linneanum (Torrell), and another
___ Eophyton, Cruziana semiplicata (Salter) and some others...-..-........- 476
or een and green sandstones and. slates, with some calcareous beds at the base. .
Estimated thickness ..... PRES ay ores a eden cece ceenee s cigliet Fekkai 1, 426
Kelly’s Island sandstones and shales. A few fucoids were the only fossils

(p) Black slate or shale, At Fortune Harbor this division was found to contain
‘ at SNE DUARLIE 825 25d. 0 5 dp i asain 2559 vaaabe soe week peanesdne. Sok 150

Be Hasinated argillaceous shale, as at Topsail Head. The fossils are Para-
pi _ doxides bennettii, Conocephalites gregarius, and probably some other species
og not yet recognized : ee PiaSe ue Ghee ute WER EN des CBee Lene ted 1, 045

uence and distribution of the rocks of the great Northern Peninsula. Geol. Survey New

nd, Report of progress for 1864. Revised edition, London, 1881, p. 15.

t ray, Alexander: Of Primordial Silurian and Kelated formations. Rep. Geol. Surv, Newfound.
nd ee, St. John’s, 1871, pp. 36-39. Geology of Newfoundland,1881, London, pp. 237-239.
Bull, 81—17

aa P Res ‘4
| ss ete - . e :

et day

soe (m) Hard, thick beds of evay and sometimes reddish imeRotie): Two species

~

Soe Seas ek wae Nat oe Oe an
“F a Mess pr eces — Rees a a ye ee

> Zs re f sn 4, = , a,
958-55 * mean, “ CAMDRIAN. 2 Naa ae ee
" ae Tb : a. _ 7s Pha ee ee
“¥e. ? on Wy oe 6 P43 uty eet
rn - 2 "2 % : ‘ =F > hg » oe

- Newfoundland for 1868? a section is given of the strata of Sey

- of Conocephalites have been recognized by Mr. Billings, and a small ee
fragment supposed of Paradoxides from a loose stone at Topsail Head; =
~ also Salterella and Crania labradorica. Thickness at Topsail Head...-.. 100

3 (l) Red, green, and blackish argillaccous slates. A few remains of trilobites :

were found at Random Island, one of which resembles Bathyurus grega-
Feud Coillitigs? jo 2c tse42 ete sdsancees eat oe apes Pee ener ok ++... om
(k) Conglomerate of Manuel’s Brook, not recognized elaewhere .:.....3scdssea =
(j) Red and green argillaceous shales or * slates. Thickness at Brigus South
Fea 2 55 cn an whe oe ow de 'gneceencentesat dee neh =ns qivas® me eaas eee ee «ss ae

(i) Red and flesh-colored limestones, in which some obscure fossils have been
found, and an Archxocyathus detected by Mr. ‘Billings. i ae

i. =

Gi). Rod plate <51- Jae. 0-slos eu nsas teow--+ bor Snneee neater} saan ceseenees BO
(g) Thin bed of impure red limestone .... .....- +200 -22 2 ee ene se eeseseccecsece §6 1D)
(f) ied MAb: a oho Paces athe So evan ss 2s ee bis Pe eXet ane teen twits 2's Som Geekbae e
(e) Red, green, and gray sandstones, tiie occasional beds of conglomerate. The — e 2g

upper beds flaggy .... . 22. Loca sc owas sncwse cece seeees fon nani aeined reer s % 30
(d) Green and reddish brown or purple slates, with smooth and regularly par- — 33 &

allel cleavage, independent of the bedding; splitting into slabs under
3 halfan inch thick. This is the position of the workable slates of Smith’s —

Sound and Random Island... iN... 2 ce weesca + cece spaeusweeeewe 137.
_(c) Abed of impure flesh-colored limestone ..5.-5 ..06e2- © nwctes stbaweewde a :
(b) Green slate, same characterasd@ ..-.......-- ay yan meee 4546 eF0
(a) Hard, dark green-gray sandstones with slaty divisions, the sandstone beds ee
varying in thickness from 4inches to 1 foot ....-......-. wa rccececcccenee 600

Total.... Oe ee phim ora a ele 5

On page 160 of the reprint of the report of the Geological Survey

Isle, as follows: 4 = a
ASCENDING. Fe ae fe

(1) Black or dark brown shales, with thin beds of sandstone from 2 to 6 inches
thick, of a gray color on fracture, mica being thickly disseminated in both
shales and sandstones, and especially at the division of the harder mem-—

DOES, vac nn sinew s ceo é Jenn Det awa in pln beads Seen bea eee a aras oe —
(2) Thin bands of sandstone like the preceding, weathering & rusty brown colon,

and divided by layers of.black shale. ...... 2.2.2. 5..2ecee eee seen ee eee <2
(3) A hard, strong bed of gray sandstone, with conchoidal fencbaies irrégularigeae

-bedded, avorage thickness about ........ 2-2... 5s2. ses ee ee cceeceenee ee 4

(4) Alternations of black shale and sandstone towards the top of the vertical
ee PCM GRE) GREENE hire 5: oy ey Ree Speman ET ‘5
_ (5) Aheavy mass of strata, mostly sandstone, forms the crest of the cliff.... anal 1

(6) Alternations of very micaceous gray sandstone and shale, the former mostly.
thin-bedded, varying from 1 to 6 or 8 inches, with Cruziana in great profu- ;
sion on many surfaces, Nodular concretions, holding Tingetias among the,
PRAISES ved Pad ade bide hon cat akepese a aee 6 ee Uh gels hen eee Pes |!

(7, ) The upper strata are a good deal concealed, but beds of sandstone occasion-

- ally crop out.on the bed and banks of a small brook near the line of section, a
some of which is of a pale yelonues color, in some cases nearly a foot thick,
pata nisi ch phen eben obec dee Siguaeetexue ne Pe ssin : M woe ---eee PS soos

JMurray, Alex.: Of the sequence and distribution of the formations. Report A the ge ologic
survey of Newfoundland for 1868. St. John’s, 1868. Revised Bate 1881. » Foe, So. hee Da

; = 3 PSN me) Se a D
. tk my) <a * hl ot or eA See

‘e en re " SUMMARY—NEWFOUNDLAND, 259
. 5 We a ie ’ ex a
Rea '. Feet.
(8) pam he upper stratam is ‘alsoh in great sat concealed, but large, angalar-jointed

- fragments of it are abundant on the surface all along the summit level,

~ which a are clearly in place, or only slightly removed. Some of these beds
q = appear to be from 1 to 2 feet thick, are rather coarsely granular, of a grayish

> pr. greenish color on fraeture, and contain crowds of organic remains, chiefly —
pa aperies of a Sa Estimated Pe CU SPE dena. Wn os Randa cep gaepere Ere

»

4 E & Total. . | a eee oot salts coateut ce dad ands ps ens uéandueoee 476

ah = 2 of this section I found, in 1888, a small species of Lingula (?),
@ ant remains of Cruziana, and an entire specimen of Oienus. Nu-
er ous trails of annelids occur on the surfaces of the sandstones, from
| ne to six, inclusive.
Mr. E. Billings described the fossils Optainéd by the Newfoundland —
_ urvey from Great Bell Island and named Eophyton jukesi, Arthraria.
atiquata, Lingula mera, Lingulella ? affinis, L.? spissa, and Cruzi-
na similis.)
In the upper portion of No. 6 Lingula murrayi occurs in considerable
lance, and from No. 8 a large number of specimens of Lingula
were collected; Hophyton linneanum Torrell and Arthraria an-
ata occur in Nos. 3 and 4,
ere is no detailed section given of the strata of Little Bell Island.
section, as determined by the writer in 1888, is made up of dark
laceous and sandy shale, with beds of gray per dark sandstone, _
oth thin-bedded and in massive layers. In the argillaceous shales.
Lingula billingsiana i is very abundant and ranges through about 150 feet:
f st rata. Toward the summit of the section on the west shore of the
is) sland a species of Hyolithes, and a long, slender shell, that may be
provisionally referred to Lingulella, occurs in a light gray sandstone.
A - few y feet. below this horizon a new species of Lingula was found in a
aceous sandstone associated with the Lingula ? occurring below in.
oe ere a
All the strata of Little Bell Island have a dip of about 7° westward
ward Great Bell Island. If this dip be retained and the section be
ee, the higher beds would pass beneath the strata on Great Bell
, at a depth of about 1,200 feet. Dr. Murray in the generalized
ct feo mentioned, has given a thickness of 1,426 feet for the strata of
it pric Bell Island and that concealed beneath the waters of Concep-
ion Bay before reaching Great Bell Island.
A detailed section of the strata of Kelly’s Island of what appears to
@ the same series as on Little Bell Island is published by Dr. Murray.? —
all Lingula (LD. billingsonia) was found midway of the 713 feet of
ti 2 I found the same species to be very abundant in the shales of
ne | ower portion of the Little Bell Island section.

i,”

<

1 ~

“ay
wm fossils from the Primordial rocks of Newfoundland. Canadian Naturalist, new ser., vol,
oe

sequence and distribution of the formations. Report upon the geological survey of New:
- cin St. John’ ’s, 1868 ; i ecceatoe aan 1881, pp. 157-159.

oe bo. ye 1 ees far a) Gu - 7 +
’ aie: eat ee Pa AS Ba ok ri ae ese eee nT ae ae ee ee € geet ar
. ie ; 5 + ch ae 4 “ S" aa ~ aot me a ~ Sa rx ; a Be % oe .
’ : = nat - a As Gat, “Se STS ; Ss, betas
260 SO SS a Se CAMBRIAN. RR SS CE a
| ; Ae : ad ne en ee

The section on the mainland baneath Topsail Head, Conception Bay -
was found to be as described by Dr. Murray.!. The limestone at the base
is separated from the ““Huronian” rocks by a fault line. Over the lime-
stone 100 feet or more of greenish shale completes one section. In the
limestones were found :? ;

Obolella atlantica, Microdiscus speciosus.

- Kutorgina labradorica, _ Microdiseus, sp. undet.
Scenella reticulata. | Olenellus (H. )bréggeri.
Hyolithellus micans. Avalonia manuelensis, ~~
H. micans var. rugosa. Solenopleura bombifrons,
Hyolithes princeps, os Agranulos (S.) strenuus,

impar. _ Agraulos(S.) sp. =

In the superjacent green shales a few fragments of a trilobite were
observed that indicated bf a portion of the glabella and eye-lobe a
large species of Paradoxides. The evidence here obtained of the rela-~
tion of the Olenellus and Paradoxides faunas being somewhat. incon-~
clusive, the section at Brigus Head, on the west side of Conception Bay, ©
was next examined and found to be essentially the same as that at Top
sail Head, with the addition of a greater thickness of green and red _

shales above the limestone, and a sandy deposit beneath the limestone
which rested unconformably against the “Huronian.” ‘The limestone”
series is divided into three bands. In the lowest, a specimen of Ayo
thes impar was found, similar to that in the limestone at Topsail Head;
associated with fragments of Olenellus (H.) briéggeri, Microdiscus helena”
and Ptychoparia? sp, (?). In the second bed of limestone, fragments of
trilobites were seen; and in the upper bed Olenellus (H.) bréggeri and
Agraulos strenuus make observed, the latter in great abundance, No
fossils were discovered in the superjacent slates. ae
_ The stratigraphic succession on Manuel’s Brook, as measured by x me
in August, 1888, is as follows :3

MANUEL’S BROOK SECTION. ~~ «

(1) Coarse conglomerate, in massive layers. The material next to the gneiss
varies in size from bowlders of quartz and gneiss 6 feet in diameter
down to small pebbles, and in the upper beds from pebbles to fine sand, am

Strike N. 80° E. (Magnetic) ; dip 12° to 13° N. es

(2) Irregular beds of calcareous sandstone, siliceous limestone, and greenish-
colored argillaceous shale, Cpr erinE the irregular upper surface of the
eonglomerate:.. =... .Vccivxwssae tages cbices saswen tnt ney eeee beeen ene 0 to 2

Fossils: Obolella atlantica, Hyolithellus micans, Helenia bella, Hyo- —
lithes princeps, H. impar, H. quadricostatus, H. similis, H. terranovicus,
Scenella reticulata, Stenotheca rugosa,varietics acuta-costa,erecta, levis and
pauper, Platyceras primavum, Microdiscus helena, M. speciosus, Olenellus _
(H.) bréggeri, Avalonia manuelensis, Agraulos (S.) strenuus and var. na- |
sutus, Solenopleura bombifrons, S. harveyi and S. howleyi._ {y

1 Op. cit., p. 154 : —
2 Walcott, C.D: Stratigraphic position of the Olenellus fauna in North aioealos and fess d An

Tour. Sci , 3d ser., vol. 37, 1889, p. 378.
2 Op. cit., pp. 380, 381,

; eh eon. a Seiad te S ait la es, S
. “eee ae ES ae hy eh
eee” SUMMARY —NEWFOUNDLAND. | 261
Cre CP ee a
anes : Feet
reenish argillaceous shate, sadthacapiy subjacent PDA Birabict acs. axe ‘ 40
) ed lish- ern MP ACOOUS BUR 1.0. oc cose neta Quicwms cece coceeuerecce " 4
3) C ‘alcareous sandstone, with pinkish limestone in irregular MaASsses...-<-- 2
5) Green argillaceous shale with thin layers of hard, dark, ferruginous sand-
& ss ‘Stone, interbedded at several horizons ...........--. POSE aii searches Y 270
Strike N. 80° E.; dip 12° N. .

Fossils: Near the base the head of an Olenellus was found ; also frag-
ments of an Agraulos or Ptychoparia. At 218 feet from ‘ie base a
Piacat of pinkish limestone contained the head of an Agraulos, like 4.
& strenuus, and many fragments of trilobites. Fifty-two feet higher up
quite an abundant fauna was found, and the following species were
collected: Lingulella sp. a., Acrothele matthewi, Agnostus sp, a., Agnostus
sp. d., Paradoxides hicksi, Conocoryphe matthewi, and Liostracus sp. a.
t) Dark argillaceous shales with thin layers of limestone and sandstone at
TONS. 00 ol Sos Vie iein ida Wh tin a'pu wade oa coease cess te cada a 295
4 i _ Fossils: Zone A: From 10 to 20 feet from the base the following spe-
4 cies were collected: Lingulella sp. a, Linnarssonia misera, Acrothele
— matthewi, Hyolithes sp.a, Agnostus 3 sp.a, b, c, Microdiscus punctatus,
a - Paradoxides hicksi, Conocoryphe (C.) matthews, C. elegans, Agraulos socialis,
- and Liostracus tener.
_ Zone B: Forty-five feet higher the fauna i ismuch larger and includes :

os

8 Linnarssonia misera, Lingulella sp. a, Orthis sp.?, Slenotheca sp. ®, Agnos-

tus punctuosus, Agnostus 5 sp. b, e, f, g, h, Micr nati punctatus, Paradox-
tds davidis, P. hicksi, Paradoxides, sp., Anopolenus venustus, Conocoryphe
vg Sastins, Ctenocephalus maithewi, Erinnys renulosa, Ptychoparia robbi, P.
_ variolaris, Holocephalina inflata and Agraulos socialis.

From 235 to 250 feet from the base a belt occurs in which a smal?
& _ species of Aristozoa occurs in large numbers, associated with Lingulella
_ sp.a, Agnostus sp. 4, and the heads of a small Ptychoparia? sp. undet.

3) 3) Alternating bands of dark shale and dark, compact sandstone that carry

~ asmall species of Orthis in large nambers.-. <2... 6. 2.20.2 e eae nce 400
oe .

TT i e section i is here cut off by the shore of Conception Bay.
a oy fauna of No. 2 is essentially the same as that of the limestones

a seneath ia conglomerate beds of Manuel’s Brook and between them
nd the subjacent Archean gneiss, there is, according to Messrs. Mur-
7 ay and Howley, a series of red and green sandstones, conglomerates
a d massive sandstone strata, which, according to their tabulated sec.
ion, have a thickness of 1 ,800 feet. They are. exposed on the north
i ot’ Trinity Bay and partially on St. Mary’s Bay. I think we should
ave more data before deciding that this series of 1,800 feet is really
ubja jacent to the Manuel’s Brook conglomerate; although it is extremely
rob: able that such is the case, judging from the SEEERIET of the Trin-
ty Bay and Conception Bay sections.
On ‘the islands in the bay the Upper Cambrian horizon is well devel-
. In the lower arenaceous shales at Lance Cove, on Great Bell Isl-
were. found Eophyton sp. ?, Cruziana semiplicata, Arthraria anti-
, Olenus sp. undet., and at a higher horizon, near the center of the
, Lingulepis affinis and Lingula ? murrayi, with fragments of Cru-

y

A y ¥ siete tiene 2 | = ; = ae ep Ff teeS . we i
sy Ree Se Ss 7: “THe “CAMBRIAN.. ees Ste

broken up to the summit of No. 8, and the strata are conformable « and

Paes ~

ziana. th the sandstone’ at the ‘summit of Little Bell Island, 20
above a band of sandstone earrying Lingula ? billingsiana and an elon- n-
gate, narrow species of Lingulella, a long slender Hyolithes? and a bri pac
species of Hyolithes occur. In the dark argillaceous shales beneath
i. ? billingsiana occurs in great numbers. %

The conglomerate (No. 1 of the section) was traced, just apeae of ag
outcrop of the gneiss, a mile to the west of Manuel’s Brook, and tl ihe
shales and limestone of No. 2 were seen in a number of sections, rest
ing directly upon it. On the brook the stratigraphic” succession 1s uh n

undisturbed with the exception of ‘hes dip of 12° to the north.

The Manuel’s Brook section is the only one known to me on
North American continent where the typical Olenellus and Parndoxidel
faunas occur in an unbroken stratigraphic section. The oa ‘
fauna is well developed and typical, and the same is true of the Par
doxides fauna. “a

As shown on the Avalon Peninsula the early Cambrian Sea iranagnl sed
across all the pre-Cambrian rocks, including the Aspidella slates and Sig.
nal Hill sandstone and the great series of altered slates and sandstones .
and, subjacent to them, the Laurentian gneisses. This sneonionniaay |
of a similar type to that between the Algonkian formations of the La
Superior and Adirondack regions and the Upper Cambrian sandsinal 2,
In each, three groups of rocks have been deposited and subsequent ntly
elevated by an orographic movement and eroded before the depositio 5
of the Cambrian sediments. The relations of the Cambrian and - pt
Cambrian rocks are all well shown upon the geological map— of t
peninsula of Avalon, Newfoundland, 1881, prepared ae Mr. James I
Howley. . . ee.

NOVA SCOTIA, a

It is very probable that the Cambrian group is represented int th
gold-bearing slates of the Nova Scotia section, but as yet the ont
means of correlation is the supposed stratigraphic position. The prit
cipal details and arguments for including this series in the Conia an
have already been given under the historical review. (Ante, pp. 56-4
It may be that they represent in large part a pre-Cambrian, Algonl id
group equivalent to the St. John slates of N ewfoundland. ae =

NEW BRUNSWICK AND CAPE BRETON. a

Our present knowledge of the Cambrian geology of the area undél
consideration is obtained from the reports of the Geological Survey y
Canada, and the numerous papers on the geology and paleontology y
southern New Brunswick by Mr. G. F. Matthew. ae 4
- Inthe report of the Geological Survey of Canada. for 1870-71, ad de
tailed description is given of the geographic distribution of. the § S
John group (pp. 134-143); and other details are added in the rep
for 187879 (pp. 6D-8D). From these reports and the map accom mp

. i
< 3 ie
. Sm

6 tlt Leah va, ghey ONS Ge a 7 er oy Aft. «F¢ nr ty a ee ee ‘. Pe
Vary? Fie fees oe. ae ar Ciches Pakage wet ee a Fig ares ie: ae eno 7 — An

-¢ -

ae ‘relating to the St. J ohn terrane. _ He says:!

ql The strata of the St. John group fill a number of narrow, trough-like taatun lying
between the Bay of Fundy and the central carboniferous area of New Brunswick.

nd it is here also that the life of the period can be studied to the best advantage.
e St. John basin lies diagonally across the ridges of Huronian rock that are found
in the eastern part of St. John County and touches the ridge of Laurentian rocks
ths rant divides this county from King’s. As might naturally be expected, the coarser
se fi iments found at the base of the St. John group are largely derived from those
Ider rocks, chiefly the Huronian; and the line of division between it (the St. John
gt up) and the Huronian formation i is marked by conglomerates of mechanical origin
which show no trace of the hardening process by which the Huronian conglomerates
anc € breccias have been so firmly cemented.

part of the St. John Basin, under the lee of the high ranges of Huronian hills which
e: st in. that direction. In Portland and the city oF St. John, at the western end of

ascending order : ‘ ‘
2 Si ; 7 - Feet.
vision ei :
tn: Red Conglomerate—wanting at that part of the basin where this sec-
tion was made ........-2... 2-222 ne eee ne cree cone cee nee nee eee
x (6) Red and green sandy einige tet Sad dee Asta Vena ap seebdaateaaeasphk BESS 150
t D ivision > Sat
. (a) Coarse * gray § sandstone or ‘quartzite Pere Pe Pe eye SS eae Aone ee 50
_ (b) Coarse gray sandy slate (Linguloid shells)..--....---..---+.------..-- 50
a) Fine gray and dark gray slaty shales (Trilobites, etc.) ............... 25
- (a) Fine black carbonaceous slaty shales (Trilobites, etc.) ................ 75
Di ision 2:
a Bee). Dark gray slates with thin seams of gray sandstone ........--..----. 220
= — (b) Coarse gray slates and gray flagstones ..-.......--..-----.-----.-- oe) B00
Bet 6) Gray sandstones and coarse slates (Linguloid shells)........---....-.. 130 .
I Jivision 3: a
(a) Dark gray finely | laminated slates........ oy Cee Be re ee eer oe 450

vision 4:

Slates and flags, resembling 2a and 26 (Linguloid shells)...--....--....... 800
Di vision 5: e ‘

| Black carbonaceous slate like, 3b (Orthids, Trilobites, ete.)..... gf ee ore 2. 450

Jeyond Division 5 the beds are supposed to be repeated by an overturn, and havea
ith across nearly vertical measures of 3,000 feet. Owing to this folding of the
asures there is some uncertainty as to where the summit of the formation i is, and
section given may not include the whole series of deposits. The faunz of Divi-
[: rf ns 2 and 5 are very imperfectly known, but there are much larger species of Lingu-
4 oid shells in these divisions than in Division 1, and the orthids of Division 5 are
cit ferent from Orthis billingsi of Division 1. ‘

“ an y he Conglomerate at the base of the St. John group marks the time when the sea of
| the Acadian epoch invaded the valleys of the Huronian formation near St. John. No
tra ice of life has aes been found in these coarse sediments, nor in the red and green

aan aes aes maid ‘oSswiex. A poe bai .

ese basins, that on which the city of St. John is situated is the most important,

~The Conglomerates of the St. John group are most fully developed in the eastern

ay Black carbonaceous and dark gray slates, less fissile than the last...... 300

2,900 -

pa Be

ui

We

© ee af ro P 5. . rye ty aoher: Wr 2 fs od aA . ee a3 .
p a - = “he > ’ gt , i k ts z . “ § Shee 4 ries ‘ - aie. J I.
264 | ae) STH CAMBRIAN. SS uscreie gh t! at ie Epes, rE

slates into which they pass. » fer the Pe mud of which these ae, are com=
- posed was deposited, an abrupt change took place in the character of the deposit, and

_ linguloid shells of several genera. Such shells become more abundant in the upper

_ tracing the sandstones westward for half a mile they are found to change into a gray
_ depth of water in this sheltered area soon encouraged the growth and multiplication — .

_ of the crustacean fauna. As the sediment which settled tom the sea water in this

is much affected by slaty cleavage, and the fossils are so much distorted, especially —

the veulney of southern New Brunswick, by L. W. Bailey, in 1865, this |

\

white sands were evenly spread over the whole basin. It is in the upper part of these
sands that one meets with the earliest traces of primordial life. These first forms. are |

part of the white and gray sandy beds, and were evidently littoral species, ag on

slaty and pebbly deposit—evidently an old beach line—and finally disappear.
Probably the physical condition of the St. John Basin at this early period was un- A
favorable to the growth ofthe trilobites; but the land was sinking, and an ad ditional |

deepening bay became finer, the remains of marine animals were preserved i in greater
numbers and variety, so that in the layers of fine slate in Group e of Division 1, many ~
genera chacteristic of the early Cambrian age are found. a

In Group d the slaty mass becomes quite fine and dark colored, but near St. John —

in the upper part, as to be unrecognizable.

In the beds of Division 2, a return of littoral conditions, and the influx of sand,
interfered with the prosperity of the crustacean fauna, and as in the lower sand beds
of Division 1, linguloid shells become the prevailing fossils. .The Paradoxides which Ta
will describe in this article are those of the intermediate mud beds, now converted.
into.a mass of slaty rock (Division 1, c).! . a

On the evidence of the contained fauna, Mr. Matthew correlated the
fauna of the Paradoxides zone of the St. John group with that of the :
Solva group of Wales, as defined by Dr. Hicks.”

In addition to the section as found at St. John there is to ibe added a 4
series described by Mr. Matthew, occurring below Division 1, on Hanford. 2
Brook, in the eastern part of St. John County. In the report upon :

mass of sediments was spoken of as the upper member of the Ooldbrook
group and distinct from the St. John group; it was subsequently joined
to the St. John group by Messrs. Bailey and Matthew in a report of
progress of the geological survey of Canada, 1870—71, p. 59, because the
want of conformity existing between the two formations could not the
be established ; but it is now found that this series is unconformable
not only to the St. John group, but also, as had been previously dis-
covered, to the underlying Coldbrook group.’ The section is as fol-—
lows :* bs aa
_. ‘Phickness—

< in feet. —
1 (a) Coarse purplish red Conglomerate, sitae onan amygdaloidal greenstone =
(toadstone) of the Coldbrook proups.. 25.5.2 27.02 0.5 cacm~ enous aneee ~ 60
(b) Gray and purplish flags and sandstones with worm-casts, seaweeds —__
(Palzochorda and Buthotrephis), and numerous spicules of sponges... 70
(c) Purplish red sandstones, with greenish layers. Remains of seaweeds : :
(Phycoidella), animal tracks (Psammnichnites and Helminthites), —
worm-burrows (Arenicolites) ©t¢.: 22... --2-. .2s ene cece ne enone se ecweee 2 ; 0

10p. cit., pp. 87-89. :
- 2 The geologic age of the Acadian fauna. The Primitive Conocoryphean. ‘British.Assoc. “Rep., 54th e
meeting, 1884, pp. 742-744. Be
Ona basal series of Cambrian rocks in Acadia. Canadian Record Siibaide, vol. 3, 1888, p. 99, a
4Qn Cambrian Organisms in Acadia. ues Soc. Canada, Trans., vol. 7, Proc., sec. a 1890, Pp. 138, aa

. ‘ a > : cau ee

a tA Pe ners en: at tee

ht oe ee we es cont ae ’ : = es r
Saas - SUMMARY—NEW ‘BRUNSWICK, “iN? Sage Sol pee
Loy gaa ‘ ' (2 Sa
mala sy ‘ i : Pre Se: R Thickness
in feet.
(a) Parplish + fed Conglomerate, more friable than 1 a. ...--.2---e- saeco --+ 35

“@) Soft purplish red shales, with green glauconite grains, the upper part
firmer and more sandy, greenish gray layers interspersed especially

towards the base. Platysolenites, Obolus, Volborthella, etc .......... - 175
a3) Purplish sandy shales, with a few bands of greenish shale. Worm-casts
= ‘ | NRE pe at heitins yan bear o de dead Sawa Eh oe on See aS Gee Oe ween 300 |
a ) Measures concealed, probably of this series........ si ose Solute <maebn 320
. : 1, 200

In this series of 1 ,000 or moré feet of beds, the very oldest layers which are fine
enough to preserve organic markings, have trails and casts of marine worms, and
also contain seaweeds, one a Palzochorda or allied genus, the other a weed witha
“flat frond similar to Buthotrephis. That these beds are marine is clearly shown by
the great numbers of spicules of hexactinellid sponges which they contain. .
About 350 feet above the base, where the measures are flaggy, tracks of annelids
are again abundant. Besides the smaller trails and burrows, there are frequent —
tr tracks of a marine animal, possibly a worm, similar to the markings on the Fucoidal
3a ndstone of Sweden, which, by Prof. O. Torrell, have been referred to the geuus
i ammichnites. A very similar track, with corresponding casts, occurs on the sur-
fa aces of the purple streaked sandstones (Assise 3) of Band 6 in turer, 1, of the St.
“a John group, and a similar trail occurs as high up as the lower band of Division 2 of
that group. Above this point, such markings have not been found, though the kind
of} rock—flags and slates—is favorable to their occurrence. The flags of the middle of
; D vision 2, of the St. John group, seem to be the horizon of Cruziana semiplicata =
alter) and C. similis (Billings); but I have not found them here. :
- ‘About 100 feet or more above the horizon where Psammichnites appears, separated
fr om it by a Conglomerate, indications of the Olenellus fauna show themselves.
These consist of Volborthella (a chambered cell resembling an Orthoceras), the cysti-
dean genus Platysolenites, Pander, and a large Obolus, allied to Michwitzia (formerly
i Obolus ? or Lingula?) monilifera, Linrs., of the Eophyton sandstone of Sweden and
‘tl 1e upper part of the ‘‘ Blue Clay ” of Bautia: Some of the layers in this part of the
k eries abound in soft green grains similar to the glauconite grains of the Cambrian
Y ocks i in Russia. The paste enveloping them is red.
ae number of beds between this point and the top of the Basal series contain worm-
sts and burrows, and some have remains of small strap-like seaweeds.

m. In summing up the facts bearing on the comparative age of this part
of the Cambrian rocks in Acadia we get no aid from the typical genera
of this horizon, Olenellus and Mesonacis, but the Acadian rocks con-
F f ain other genera of this fauna which serve to fix their age with a cer-
te in degree of accuracy. Some of these genera, however, are such as
ia ay have a wider range of existence in time than the trilobites, and
Aherefore are not of the same homotaxial value. - The trilobites that do
occur are not so definitive as some others.'

In his latest table of classification Mr. Matthew arranges the Cam-
b rian ‘System as it occurs in Acadia as follows :

4

Be Localities.

A Pay D.—Upper Cambrian (Potsdam series) ..............---- Unknown.
_ C.—Middle and Lower Cambrian, Acadian series. .....St. John, etc.

: B.—Lower Cambrian, Georgian series......-....---.----- C. Breton.
> A.—Basal ace Etcheminian ROPIM Lass & comp ins St. John, etc.

— 10p. cit., p. 143.
4 classification of the Cambrian rocks in Acadia. No.2. Canadian Record of Science, vol. 3,

. eae igs Po Ls. Bes ane oi. = a. aie a, TM 2 Ww: Arg on Bg « a eS
a 5a a ‘as % hi 2 .

-

‘ ~

iy oe “4 so ta 8% had - > ta ee * bes 8 a) ee Oe ME 2 $8 Pees) os. Cait tans

Se Soe ign tp ay ee ete wo Shee et at
“s

7

' a cess Se 5 pees
all . fT- @
~~ & in Wig ® wy r Tey ayer

ee

BGR SS oe A. THE CAMBRIAN..

In Seaniblig’ in 1888 (at that time called series 5B} ihe Paradorides .
- zone, or C of the preceding tabulation, the term “ stage” replaces the —

~ word “division” as heretofore used by Mr. Matthew, and the divisions ie

of the series are given as follows 2 : ee

Saige 1.—This includes the lower part of the series as high up as Paradoxides are
found. The divisions of this stage are as follows :— 5 3
Band (assise) a. Hard gray sandstone or quartzite. Fossils, none known, i a
Band (or assise) b. Dark-gray sandstones and gray sandy shales. Fossils: =
Ellipsocephalus, Agraulos, Hipponicharion, Beyrichona, etc.
Band (or assise) ¢. Gray shales. Fossils: Paradoxides, Conocoryphe, Li- 4
ostracus, Microdiscus, Agnostus, etc. : 4
Band (orassise) d. Dark gray shales. Fossils: Paradoxides, Ptychoparia, 4
Solenopleura, Microdiscus, Agnostus, Stay, of different species from those | 3
in assise ¢. me “y
Stage 2. —This consists of gray flags and sandy shales. The subdivisions have ‘not |
been worked out, but the stage corresponds to the lower half of the Olenus ©
zone in Europe. No species of the genus Olenus have been found in it.
wiave 3. —Dark- -gray and black shales. Fossils: Ctenopyge, Kutorgina, Orthis, ete.
This corresponds to the upper half of the Olenus zone of Europe. The
shales in Cape Breton, which contain Peltura and Spheropthalmus, be- — 7
long here. There are in the St. John Basin gray flags, which overlie the af
- Ctenopyge beds, but no higher stage than the Olenus zone has been estab- —
lished by fossils.? :

Wy diy

In a series of sections of Cambrian ee in Acadia,? the upper Cam- |
brian or Olenus beds are shown to be present. in St. John County i in the
Portland section. : 2

Just as this report is going to press (May 1, 1891) 1 received the fifth e
contribution of Mr. G. F. Matthew upon the fauna of the St. John —
Group. In the introduction he gives a description of the structure of —
the St. John basin and sections of the measures at St.John. He finds —
that all three of his divisions of the Cambrian are present. eves i

_be names Acadian, Division 2 Johannian, and Division 3 Bretonian4

The Cambrian rocks of Cape Breton Island are described with many
details by Mr. Hugh Fletcher in 1877 and 1878, but the various outcrops —
do not appear to have been well correlated. The section in Moleata
Brook, on Little Bras d’Or Lake, is as follows si

(1) Carboniferous conglomerate and related yogks ssc: Fataneianpes see Ree

(2) Feldspathic sandstone and impure limestone, of white, green, amber, red, _
and otber colors, mixed, and in distinct beds of different thickness ; some-
times associated with esteniate soft, soapy rocks, probabl y desabnanee fel-
sites; films of hematite in the WOMEN. isk tba op 5 = Bane sa aie top oa rae 25s i

SS

Fedina't in the St. John series, thus catablishinge the Be of the Lower Siijurian (Ordovician) faut : ;
above the Olenus zone. -

8Matthew,G.F. On the classification of the Cambrian rocks in Acadia. No. coe Canadian Rec. Set, ;
vol. 3, 1889, P. 308.

p. 129. a
6 Report on the geology of part of the counties of Vivtoria, Cape Breton, and Richmond, Nova Sco.
tia. Geol. Sur. Canad. Rept, Prog. for 1876-'77. Montreal, 1878, p. 431. ; :

~ x
/ ' z s

Pat hele” i

fat —_ hires ta Ase: Sty > : v2 >> 4 Sa i
ig RGA aire sone —aane. SR as Dy ae
‘228 aa 2. <f ~ any A = r
ee = | ; Feet. ;

) Blackish end, gray alata: Rad ae tae, and argillaceous limestone ; also, > .
compact, feldspathic rock, ears with limestone of different colors, Not
= MINS So Sit so ite ae ee ne T's 9's ts od dna ip bo tapevee save one, 84
“ia ‘Dark and pale gray slates, with thin layers of quartz, spotted =e iron :
pyrites et AMON TOL RONG cs Oso 5 wile an oe a sds gare a bye Se aacwnsa on beating 66
© Greenish gray, fine- grained, pyritous rock, resembling sandstone and yield-
--_—_—_—sing easily to the EI ER fait agi na an Sa cada s Wo sk abies nm aad can aeoahes 19
6) Black and gray argillite, full of small twisted layers of quartz, which are

- - sometimes so numerous as to constitute an impure quartzite, spotted with

a ‘te ae z pytites. Associated with and overlie dark- sini pippbaginoas argillite, =
aA Se COE DN TICOUN COBLOUC IRVOUS 2 5. cen deine a soe shee nae e ton bes beaene 65
(7). Bluish-gray, pearly, papery slates, cleft in every direction and traversed in

the bedding and across it by streaks of calespar and quartz .-.-...----. 30
*e (8) Bluish felsite, crystalline limestone and quartz, confusedly mixed in con-
pe i a el a Pe renaia os Lele hs wathan ax ieee 37
(9) Bluish-gray coherent argillite...........- Rein Sins 7c Relea Dae wie Weed pene re 60
> ae Greenish, decomposed, feldspathic rock, of uncertain thickness ........-. 110
ae Red syenite in steeply rising hills..... Nagh Ma eddie ae pad nt wk eee wi tee

Ga pag y 15
ee The Peabsian rocks occur as long narrow areas resting on the subja-—
% - cent Laurentian rocks, as shown on the map accompanying Mr. Fletcher’s
_ report of 1876-7 7; and on the map accompanying the report for 187 5-7 6.
In the text of the latter report the rocks are described as they occur on - =
«St. Andrew’s Channel, and the geographic distribution is given on the ~
map. From a small Scdoaien on the Mira River a collection of trilo-
bites was obtained that indicate the upper Cambrian fauna. They in-
elude, as identified by Mr. Matthew, Peltura scarabeoides, Spharophthal-
mus alatus, and Agnostus pisiformis.| It is not certain that all the rocks
% referred to the Lower Silurian by Mr. Fletcher belong to the Cambrian -
_ group, but as far as known all the fossils that have been found indicate
a et the upper Cambrian series.

- MAINE,

ie: “The presence of typical rocks of the Cambrian group in = ie State
of. Maine i is not yet proved. It is quite probable, as in the case of Nova
2 Ss otia, that the series of slates referred to the Cambrian actually belong
ab that horizon. But until paleontologic evidence is obtained, the
Bapestion will be an open one. The stratigraphic position of the slates
and d their lithologic character enable us to speak of them tentatively
a s belonging to the Cambrian group. That they were deposited in the.
me basin as the Cambrian series of New Brunswick and Massachu-
S tts i is not Eropabre.

* NEW HAMPSHIRE,

a all the references of strata to the Cambrian group in New Hampshire

are eof a provisional character. They are based upon more or less im-
ae ‘

tn mn the Cambrian faunas of Cape Breton and Newfoundland. ae Soc. Canada, Proc. and irae
vO al. 4, nec. 4, 1887, p. 147.

a
a

4
ioe
dew

=a

me,

=

he _ a prominent part in the composition of the conglomerate, especially in the central

__ these rocks, they are either typical clay slates or slightly calcareous; but along the a

~

_ suggested an inferior position for them. They may be called Silurian,

‘and the age of these is certainly and definitely known only at the Paradoxides quarry, x

oe ae age cat ee oy eT AS oe eee = Sis A ap Re Dl
Bega Sep oa Ae 3 CD nga oes
7 " 4 F ~ t+ sy ; 7 on <8 aig oS P Reed Ve ria» < = a 3 Oy
ae ® - is a eyo “hr ae sh Ne 3 xe
e), ‘ \ . ~ : 7 _— = Pa - ae >t
rE CP Ce ry eee “THE CAMBRIAN. aS: oS Pawn. we
in ; ae ik ey eA oo ae

perfectly determined stratigraphic noise and the fact that: there i “8
a thick mass of sediments, usually without fossils and largely sraille
ceous in character, that appear to be pre- -Silurian in age. By their lith- |
ologic character they are correlated with formations referred to the
Cambrian group, as found in Maine and Nova Scotia, that have similar _ yo
- lithologic characters and occur in a similar stratigraphic position. | All
these doubtful formations are in turn correlated by their lithologie char-
acters and supposed stratigraphic position with the Cambrian beds of —
Newfoundland and New Brunswick. ~

In speaking of the Mica-schist series of New Hampshire, Prof. ©. H.
Hitchcock says! that there unquestionably exists an enormous thick-
ness of mica-schists in southern New Hampshire above the Huronian
series. ‘No author who has devoted any attention to these groups has - A

Cambrian, or pre-Cambrian, according as each author is inclined to re-—
gard New Eneteod, very dicieak or on the verge of the Paleozoic.” F
It is doubtful if these exposures should be referred to the Atlantic
Coast Province. It is done at present as a matter of convenience.

EASTERN MASSACHUSETTS,

The description of the Cambrian rocks of the Boston Basin, by Prof.W.
O. Crosby, is the most recent-and the most thorough of any we haven
and the summary of our present knowledge of them is taken mainly =
from his paper. He says:?. 3 2 4 q

The oldest: rocks which we have found are the Primordial slates and quartzites, a ;

in Braintree. We appear to be justified, however, in regarding them, provisionally —
at least as all of about the same age, partly on account of a general lithologie re- J
semblance, but mainly because their relations to the different classes of eruptive —
rocks are everywhere the same. In Weymouth and Braintree, where we first met _

northern base of the Blue Hills occasional layers are distinctly siliceous. They prob-
ably underlie a large part of the Boston Basin, being covered by the conglomerate <a
and the newer slate; and north of the basin, as shown in the ninth lecture, they —
occur in isolated ar Sis among the eruptive rocks.- In some of these areas, especially — 7
in the Middlesex Fells and Melrose, and in Woburn, clay slate similar to that in ae
Quincy and Braintree is repeatedly interstratified with quartzite, while toward the — .
southwest, in Natick, and also in Reading and Lynnfield, there are extensive develop-
meuts of quartzite swith little or no slate. Itis very clear that the quartzite north —
and west of the Boston Basin is the source of the quartzite pebbles which play such —

- and northwestern sections of the basin. In general, the quartzite is more and the —
slate less abundant northwestward, indicating that the ancient shore line along —
which these strata were deposited lay in that direction, and originally the Pri mordial
strata were probably spread continuously over all the region to the southeast of e
that line. ~ er

—

' Geological sections across Vermont and New Hampshire. Am. Mus. Nat. Hist. Bull., vol. 1 , 1884, Dad
168, 2 a
2 Physical History of the Boston Basin. Lowell free lectures, 1889- 1890, Boston, 1889, pp. 19, 20, as

Ba
- ; ae

aa m - 55 uae aie iti ae ea a eee, Oe Ss Sa tas : x Ny c “3 Meek a
a ie ulucioaberss. ss 269 -

ier
SAP

ti rown into sharp folds having, in general, a northeast and southwest direction. This
“appears, also, to have been a period of intense voleanic activity. The quartzite and
slate were shattered and isolated by great volumes of basic lava, which we now call
: _ diorite ; and, as indicated by the compact and scoriaceous diorite of the Middlesex
Fells and other localities, immense floods of lava were also poured out on the surface,
~ concealing the sedimentary rocks. In breaking through the quartzite and slate, the
- diorite has often followed the planes of stratification in those rocks, and thus appears
_ in many cases to be regularly interstratified with them ; and this bedded appearance
Fe of the diorite is greatly increased by the very perfeet aw -sisnetins which was de-
ture sometimes resulting from the subsequent action of both mechanical and chemical
forces. We are thus able to explain the fact that the diorite has been pp i
mistaken for a stratified or sedimentary rock.

= ~The eruption of the diorite was probably followed by a prolonged ‘dani of aniet

and long continued igneous action, during which only acid rocks—the granites and
& felsites—were formed. Allover this regionthe granité has broken through the Pri-
a mordial strata and the diorite in the most irregular and intimate manner.

: ~ the eruption of the rocks occurring as dikes the series was raised above
- the sea level and subjected to long-continued erosion, prior to a down-
_ ward movement or subsidence. As the surface passed slowly below
the level of the sea a thick bed of conglomerate was spread over the
; earlier series of rocks and_a fine silt or clay carried out into the deep
= = Water of the ocean. At the same time eruptive rocks were repeatedly
poured out over the sea floor, where the beds of gravel and sand were

| 3 stone with beds of melaphyr and porphyrite. ! ;
Of the subsequent depositions of sediment, he says:

& _Alternations of the conglomerate with beds of both sandstone and slate are also of
common occurrence, indicating oscillations of level during this period. But the down-
ward movement prevailed, until finally the water became too deep and quiet and
id too remote from the shore, in this vicinity, to permit the formation of conglomerate
and ‘sandstone; but these coarse sediments were gradually replaced by slate during

_ have continued for a very long time, for the argillaceous sediments accumulate very
__ Slowly and yet the slate series has a thickness of from 500 feet to fully 1,000 feet or
_" more. The slates are probably somewhat thicker than the conglomerates, and were
ie ‘ at this. time we unfortunately know but little, as the slate is very generally destitute
of fossils ; and the full chronologic significance of the few organic remains that have
been obtained from the layers of limestone in the slate at Nahant is still undeter-
4 — wined.?

There is evidently an error in Prof. Crosby’s interpretation of the
atigraphic succession of the formations he describes, as the fauna at
tant ; is of an older date than that found in the argillites at Braintree,
Ri If, however, the conglomerates, with their contemporaneous eruptive

ca, ; ‘Op. cit., p. 20. ~ 20p. cit., p. 21.
a: :

he deposition of the Primordial shisin was followed by a period of disturbance of
‘part of the earth’s crust, during which they were strongly compressed, being ©

; veloped i in large masses of it, as well as by the distinctly schistose or foliated strac-

erosion, which was finally terminated by the advent of a second period of intense —

Prof. Crosby considers that after the deposition of the argillites and

Peiimularing, thus forming alternating beds of conglomerate and sand-

a the dying out of the volcanic activity. These tranquil, deep-sea conditions must

doubtless several if not many times longer i in forming. Of the life existing in the sea |

»

‘

~ entirely isolated, and concerning its relations to the conglemerate we know nothing. I have supposed,

Bae Be! _—_ <—_—_-— aie — 4 ya Pe’. D9" ow 3 .. eae “SS > ) a" a * ae “i *. > *
St SS Lan IS ees TA en eae oe aS San eee ae ee iS NAA ae kt ae
> cans i oe ene oer Se ¥, Maho : : Sis

rosks, belong to the same series as the East Poiit slate ‘uit Timestone
the entire series must be referred to the Cambrian.

‘ %
South Braintree. Ile assigns to the conglomerate a maximum volume

in Braintree, the known locality of Primordial fossils, the slate is de- —

-marked uniformity between the conglomerate and lower slates.

2 ee | ih Ried Wiehe,

=o an : s 44 " 7 .

ie : 3 he . Tey A! Oe Se chap ae 5 Bes, UP ~
PRON a Fa Be a Rees i al. aR PR gs ont:

if a ae

PME Es THE CAMBRIAN. > aes = 4

coe

In his report of 1880 Prof. Crosby considers that the aie of the
Boston Basin were deposited in a depression excavated in the erystal-
line formations and that there are several formations belonging to the z
Cambrian. First, a conglomerate, represented by the Roxbury pudding: —
stone. Second, a slate series which incloses the Paradoxides zone in

not exceeding 1,000 feet, and considers that the greatest thickness of —
the slate can not be much less than that of the conglomerate, al though —
in some cases certainly falling below 500 feet.2 At the trilobite quarry —

seribed as of a greenish gray color, “somewhat siliceous, fine-grained, —
and remarkably uniform. Minute grains of pyrite are pretty generally
diffused. In the quarry the rock is apparently only very coarsely - —
jointed; but the weathered surface reveals much finer division by this q .
ineans. The stratification is very massive and can hardly be detected,
except by means of the trilobite remains; these may be supposed to.
lie in the plane of the bedding, and wodordieg to this indieation the —
strike is E.-W., and the dip S. 809-859. Across the strike, southerly, “
the slate, still apparently maintaining a high dip in that direction, is —
inet at a distance of perhaps 300 feet by fine-grained grayish and red-— a
dish Huronian granite, while on the west the same granite cuts off the —
slate at about twice the above distance from the trilobite quarry ; that —
is, the contact of the two formations, as shown on the map, is sisi ae
to the strike of the slate.”* On the map the slate series icone P
the Boston Basin is correlated with the slates at Braintree, and repre-
sented by a common color. f : , ea

*

1In a letter received from Prof. Crosby, dated January 27, 189i, he says: “The Nahant slate ba

however, that it should be referred to the newer Heros, above the conglomerate. ” Of the sorta
geology of the Boston Basin he says:

“ Assuming that the slates of the Boston Basin now known to be Cambrian are overlain in : succes- a
sion by the conglomerates and a newer slate series (my present working hypothesis), it is still pos- ‘=
sible, I suppose, that all these rocks, in the Boston Basin, may be Cambrian ; notwithstanding the

_ ‘The weak points in the stratigraphy are (1) the general (not entire) absence of slate pebbles in lie’
‘conglomerate; (2) the absence of clear sections showing the conglomerate resting upon a lower nie .
series. Wherever the base of the conglomerate is seen, it reposes upon the granite or felsite. Some
of the sections are very clear and unmistakable in this respect; and apparently the same granite <a
felsite are eruptive through the Braintree slates. It would, of course, be difficult to prove that the —
granites and felsites are allof the same age; butit seems best to assume that until the contrary a

_ appears. “a

overlain unconformably by the conglomerate of unknown age; and the conglomerate i in turn overlain

“The best general statement of the stratigraphy of this region appears therefore to be thige. A
lower slate, known to be Cambrian ; cut in succession by diorite, granite and felsite; all these rocks —

conformably by a newer slate of unknown age.
‘*Thechief problems are, then, to determine which are older and which are newer slates, aia to de

termine the age of the conglomerate and upper slate. :
‘‘Ags an indication of progress, we have the discovery by Mr. Wasdstortt: just reported, of fossils.

+b

.

in the slate of both Somerville and Newton.” BF a
2Contributions to the geology of Eastern Massachusetts. Boston Soe, Nat. Hist? Oocnaldaalal
papers, No. 3, 1880, p. 266. * it te oe
3 Op. cit., p. 192. : | G3 eZ ote t ee

> r . = i
a te J < P , Ae

a hl Ton <
Ra ~ —.
ee a

fen senting to Dr. M. E. Ww adsworth! the strata at the trilobite ¢ quarry
: dip a little west of south at an angleof 55°. This is nearly as given
bs Mr. Isaac Lea in 1858.2 It is quite probable that the variation in
=f ngle of dip mentioned by different observers is owing to the position
of the exposures in the quarry, at the time of their respective visits,
sf ind by their mistaking the cleavage for the plane of bedding.

i ‘Dr. Crosby® deseribes the rocks at East Point, Nahant, as composed
“of @ very dark gray, almost black, compact slate, witha strike N, 60° BE.
and nearly uniform northerly dip of about 40°. The slate is inclosed
"in, and extensively cut by, the coarsely crystalline pyroxenic rock of
the Naugus Head series. The slate, except where it is vesicular, is of ©
a uniform grayish black color and holds thin beds of linestone aggre-

a mestone and its mode of occurrence are precisely like those of Mill
Cov re, in Weymouth, 13 miles distant. The limestones are interstrat-
3 ifled with the slate and not always distinguishable from it. The color
is light gray and its texture varies from compact to finely crystalline
or saccharoidal. Thin seams and veins of siliceous material become
" een on the weathered surface.

Be In the interbedded limestones Mr. A. F. Foerste discovered in 1889
traces of a species of Hyolithes which he identified as specifically the
same as a species found in the decomposed limestones of North Attle-
of borough ‘ He proposed the name Hyolithes inequilateralis, but I think
it is identical with Hyolithes communis, var. emmonsi, of the Lower
¢ Jambrian horizon at Troy, New York. He states that the Nahant lime-
jones are the equivalent of the red slates in North Weymouth; and
| E that it is very probable the red slates and included limestones are
-stratigraphically. beneath the Braintree Paradoxides beds. Also that
og red slates of Mill Cove, in North Weymouth, are of Olenellus age
anil beneath the Paradoxides strata.
bes The district embracing the Cambrian rocks of Bristol County, Mas-
p sachueetts, is well described by Prof. N.S. Shaler. He says:

_ Several geologists have observed the fact that between Providence, Rhode Island,
nd Wrenthan, Massachusetts, we have an extensive development of interbedded con-
Sisinorates, shaly slates, and sandstones, the whole separated from the other detrital
oposits of this region by peculiarities of color. * * * Various conjectures have

been made as to the age of these deposits. They have been thought by one observer
Eto. 0 resemble the Trias, while others, owing partly to their position, have pag

“we

w them to the Devonian age.®
= Prof. Shaler discovered fossils of the Lower Cambrian or Olenellus

a one in this series of rocks in 1883, which for the first time gave data ~

¥ “TOn the elation of the Quincy granite to the primordial argillite of Braintree, Massachusetts. Bos-
ton Soc. Nat. Hist. Proc., vol. 21, 1883, pp. 274-277.
ao the trilobite formation at Braiztree, Massachusetts]. Phil. Acad. Sci. Proc., vol. 9, 1858, p. 205.
8 fee enertontions to the geology of Eastern Massachusetts. Boston Soc. Nat. Hist. Occasional papers,
No. 3, 1880, pp. 195, 261, 262. *
— 4 The Paleontological horizon of the limestone 2t Nahant, Massachusetts. Boston Soc. Nat. Hist. ~
Proc., vol. 24, 1889, pp. 261-263.

ie ) =On 1 the geology of the Cambrian district of Gristol County, Massachusetts. Bull, Mus. Comp, Zool.,

. Col., vol. 18, 1888, pp. 18, 14,
Ry a.

ty ee a
.

Pg to a ‘Rain x :
Peres: ‘SUMMARY—MASSACHUSETTS. Seeger ss 201 ‘a

“gating, perhaps, 20 feet of calcareous matter. The character of the —

\

=

iy Sie See ne ae ‘THE CAMBRIAN.

_ taken are mainly identifiable in the western portion of the field before described. catinhs,

— too, the large amount of sandy matter even in the slates affords a presumption that 4

- feet, and even in this section only a small part of the rocks actually contain fossils. 8

for Aéterninias the geologic age of the deposit. On the east ‘the Ooak

Measures of the Narragansett Basin occur. On the west side he con:

siders the rocks to be of pre-Cambrian age, as they consist mainly of

- gneissoid rocks of various composition, and a great area of dark green- 4

ish chloritic deposits which appear in part at least to be metamor- —
phosed conglomorates and shales. Owing to the large amount of drift ‘
material covering the country, no absolute contact with the pre-Cam- :
brian rocks was observed, nor is the overlap of the Carboniferous upon |
the Cambrian shown in any section. Saree
Of the rocks he says: ;

he
| 7
The Cambrian rocks exhibit very little sign of metamorphic action. The shales
indicate a slight amount of infiltration, and in the conglomerates the pebbles all re- :
tain essentially their original character, save that they are sometimes slightly in- —
dented one intothe other. The cement of the mass is not more altered than is usual
with our unchanged conglomerates. Its general characters, save for itsreddish color, _
is undistinguishable from the deposits of Millstone grit age in the neighboring coal —
fields. '
So far fossils have been found in rocks of this section which probably do not in x
the aggregate include more than 100 feet or so of the total section of the Cambrian

series. However, as these deposits are of the same aspect, as all the red slates

and conglomerates of the area, it appears at present reasonable to include all
rocks of this description with the above-mentioned series. The total thickness of ;
the section which I have termed Cambrian is not accurately determinable. It proba-
tly amounts to not far from 2,000 feet. In the main it consists of thin bedded shaly :
layers which occasionally pass into moderately thick, fine grained, greenish and red- —

dish slates. Intermingled with these in several levels we have a number of layers —
of conglomerate, perhaps as many as half a dozen distinct beds, varying in thickness —
from 200 to 300 feet. In all cases these conglomerates are frequently interrupted by —
thin layers of shale or sandstone. * * * The rocks from which the pebbles were

>?

The sediments composing this Cambrian section appear to have been derived from —
rocks substantially’ the same as those which now lie in the field west of the area. —
Although fossils have been found in a small part of the section, close study makes it —
plain that by far the greater portion of the strata are clearly azoic. The frequent :
return of conglomerate layers and the coarseness of the pebbles show that during B
most of the time when the beds were accumulating the region was near shore; so,

the region was not remote from the coast line. About 100 feet of shale beds have > %
been subjected to a very careful search for organic remains. ‘The total thickness of
the deposits in which any trace of life has been found probably does not exceed 100

Prof. Shaler suggests that the conglomerates were accumulated dur.
‘ing an ice epoch; and he presents several arguments for this view. He E
states that the relations of the beds carrying the fauna at North Attle- |
borough with those of the Paradoxides zone of Braintree are not dis.
coverable by comparison with the Massachusetts Bay and N arragansett
deposits. At the time he wrote the stratigraphic relation of the Ole-
nellus fauna as found at North Attleborough with the Paradoxides
fauna was not known, except that the Scandinavian geologists state

1Op. cit., pp. 16, 17. 20p. cit., p. 18, ®Op. cit., p. 20.

-

aa

Shes! s : cae

cs et oe "ATLANTIC coast—nésume, 3 a

> Se a a ~

at in n their country, the Paradoxides zone occupied ¢ a superior position
gra hic succession of the Cambrian faunas, the Paradoxides beds of
raintree are considered to be superior to the Lower Camyrian rocks
of atisborongh

SS

; te ;

a ‘The physical characters and condition of the sadkis constituting the

formations referred to the Cambrian in this province indicate that they
y were accumulated not far from the shore line, and that several fluctua-
tions in the level of the sea bed occurred during Cambrian time. On
Be e coast of Labrador the accumulation of sand was followed by a

=
. RESUME.

both was not profound, is shown by the character of the limestone and
Sian, and the presence of lenticular masses of red and. green shale.
The 231 feet of sandstone, and 140 feet of limestone in the section rep-

re res sent only a portion of the Lower Cambrian or Olenellus zone. Two

yr ee ence of 605 feet of slate beneath the alternating series of limestone
and quartzite, over 1,000 feet in thickness, tell the same story of rela-
tively shallow water accumulation.

— On the Atlantic coast side, at Canada Bay, there are 2,500 feet of
sk: ate, conglomerate and eruptive rock, subjacent to a series of lime-
5 tones and slates nearly 3,000 feet in thickness. There is here a greater
d relopment of Pnathans than anywhere to the south along the At-
1 E ntic coast line. It appears to have accumulated upon the bed of a
acted séa not far distant from the shore and to have been frequently
in SE crapted i in deposition by the throwing down of a considerable thick-

2 ess of argillaceous mud.

In southeastern Newfoundland the assembled sections shen accord-

ig to Messrs. Murray and Howley, a thickness of nearly 6,000 feet, of
wih ich 128 feet are limestone, and the remaining portion araitabeens
an and l arenaceous deposits. In the section on Manuel’s Brook a conglom-
= 2) rests upon the pre-Cambrian gneiss, and upon the upper bed an
| rregular, arenaceous limestone in which layers of more or less pure
astone occur. This limestone-forming epoch was of very short dura-
te aud was. succeeded by an accumulation of clay that now forms a
ies. of shales nearly 1,000 feet in thickness before sandy layers ap-

- When once the sandstones begin to alternate with the shales,
y y continue on up to the summit of the group and are very abundant
i 4 Upper Cambrian. The sediments of southeastern Newfoundland
wv es e accumulated in bays of the pre-Cambrian sea and derived almost
irely from the adjacent shore, either as sand and silt, worn from the
oks by the sea, or brought down to it by tributary streams.

7 T he 4,000 feet or more of rocks in the New Brunswick section are
ulin nost entirely shales with a few sandstones and basal conglomerates.
ae Semi Bh 18 ;

te @ .~ 2 ie OP ee ae ne « iD. es a” oe ene Oe ate on i te a ee a a Oe pe Ge So
ee aa Ree Se, 2 aut bo Oa A Fie ik Oe Biky 5
Aate © baw ; bo + 7 ire <

9 the Olenellus zone. With the knowledge we now have of the strati- |

sepening of the sea and the deposition of calcareous mud. That the .

7 undred miles to the south, on the west coast of Newfoundland the >

* !
#22

274 Zs a THE CAMBRIAN. Sega coe a3 + Pron et

—

It is the record of the socaaialation of sediments i in a gradually deep-
ening sea. ee
The eastern Massachusetts section is faspety forined of shale, except.
in the lower part, where a small proportion of limestone occurs in the
- Olenellus zone, much as in the southeastern Newfoundland section.
The great thickness of shales referred to the Cambrian in Nova
Scotia, Maine, and New Hampshire probably represents much more
than the Cambrian group, or it may be entirely a pre-Cambrian forma-—
tion or a post-Cambrian formation. It is only probable that they are of ©

Cambrian age. “They may represent deep-water accumulations in which”
no organic remains were buried. 4

As a whole, we may regard the Atlantic Coast Province, sovtaee Cam.
brian time, as including bays and the adjacent shores of the Algonkiz
land, in and along which sediments, mostly of an argillaceous a
arenaceous character, accumulated. The relative level of the sea bed
varied, but in the main the depression greatly exceeded the elevation.
The depth of water in which the sediments forming the limestones and
shales accumulated was probably considerable, but not a deep sea in
the present sense of the term. A few hundred or a thousand feet on a
gradually sinking sea bed (in relation to the coast line) would give the 4
required conditions. From the character of the sediments and the
faunas itis probable that land barriers existed to the eastward of t
present coast, and that none of the eas were accumulated off the 7
shore facing the open ocean. i
As left by erosion the Lower Cambrian now occurs on the Labrador r
coast, on the western and eastern sides
of Wewfonindiaad: in New Bronswil
and eastern Macsiolotete The Mid-
dle Cambrian has been recognized on
- the eastern coast of Newfoundland, in
New Brunswick, and eastern Massa-
chusetts. The Upper Cambrian is
known in southeastern Newfoundland,
Cape Breton Island, New Brunswick
. and doubtfully on the southwestern

Fic. 1.—Typical sections of the Atlantic

Coast Province. Vertical scale, 6,400 feet COAaSt of Newfoundland. (See Pl. wm )
to the inch. < oe

Ce

a

il

|

]
sit
| il

[
|
1
ret

Al
nll

f

Ni!

Be
3

i
q

APPALACHIAN PROVINCE.

The Appalachian Province includes the outcrops of Cambrian str ta
on the line of the Appalachian System of Mountains, from the Gulf o
St. Lawrence on the north to Georgia and Alabama on the south. _

For convenience in presenting geologic data the » Appalachian Prov.
ince is divided into: ‘a

A.—Northern Appalachian District. . 3
B.—Southern Appalachian District. a

ee "i ed
tame 4, +? eS
La 4 ? ts ye s >

_ SUMMARY—NORTHERN . APPALACHIAN, : 275

~

_ NORTHERN APPALACHIAN DISTRICT,

The Northern Appalachian District includes the Hudson River and
“Lake Champlain area, east of the river and lake, and an extension
g northeastward into Canada as far as the vicinity of Cape Rosier on ce
Gulf of St. Lawrence.
a _ The geographic distribution of the Cambrian strata of the N orthern
3 Appalachian District, south of the Canadian extension, is deline-
ated on a geologic map of eastern New York and western Vermont
published in 1888 by Mr. C. D. Walcott.1 On this map the “ Gran-
ular Quartz,” “Red sandrock, ” “Georgia slate,” and Potsdam sand-
stone are differentiated as far as the awn data would permit.

shown in a series of sections by Prof. C. H. Hitchcock, > and for New
York by a section on the above-mentioned map.
The “ Granular Quartz” is found on the western side of the Archean

to Massachusetts, and into Vermont nearly to the Canadian border. The
- exposed outcrop is more or less interrupted because of the removal of
the rock by erosion or its concealment by superjacent deposits. |

~ Jn Vermont the “ Granular Quartz” is a very compact, hard rock that

Vermont? as granular, gray, or reddish quartz rock; fine granular or
_ arenaceous quartz rock: granular porous quartz, or pseudo- buhrstone;
quartzose aggregate; quartzose breccia; quartzose and micaceous con-
_glomerate. There are also associated with it talcose and mica schists
and limestone. The quartzite is remarkably compact and enduring,
and it occurs in bowlders all over the southern part of Vermont, in
_ Massachusetts, New York, and Connecticut, many miles from the parent
| Beces: Along the range of the rocks the bowlders cover the surface,
and in some instances this is the only way in which the line of outcrop
>of the formation is indicated. Details of the geographic distribution
in Vermont are given in volume 1 of the Geological Survey. A sec-
tion of 973 feet was measured in East Dorset by Prof. C. H. Hitchcock,
and the thickness of the formation in Vermont is estimated at 1 000
set. It retains its essential characters in passing southward into
Massachosetts, New York, and Connecticut.
On the western summit of Clarksburg Mountain, northeast of Wil-
. iamstown, the basal bed of the quartz series is a conglomerate, resting
u unconformably upon pre-Cambrian gneiss. The conglomerate is suc-
; ce ceded by beds of quartzite, usually compact, hard, fine grained, and

1 The Taconic system of Emmons and the use of the name Taconic in geologic nomenelature. Am.
_ Jour. Sci., 3d ser., vol. 35, 1888, pp. 229-242, 307-327, 394-401.

s _ ?Geological sections across Vermont and New Hampshire, Am. Mus. Nat. Hist. Bull, vol. 1, 1884, pp.
155-279, pL xvi, xvii.

_,Bitencoc, H. Hypozoic and Paleozoic rocks. Reporton the geology of Vermont, vol. 1, 1861,
oi ,

2 “2s

>

' The stratigraphic relations of the various divisions in Vermont are

:

_ passes into a number of varieties. It is described in the Geology of |

rocks, from southeastern New York and western Connecticut northward ~_

-

and even up to 6 feet in thickness, on the spurs to the north of Clarks- ‘
burgh Mountain. In the town of Bennington, a few miles further”
north, the writer measured a séction of the quartzite 400 feet in thick-

quartz. At this locality fossils other than the Scolithus borings, which ©

count of the discovery, by Mr. A. F. Poersté and himself, of fossils of

~ Olenellus in Bennington County. Dr. Wolff identified the species as

contain fossils of Calciferous Chazy-Trenton age, or those which » will

Prof. Frank Nason, in Sussex County, New Jersey.

ee Ry ~~ ON es = a ee 4 FPA) it at 6 bY oa
=f | See gare Bie Beat no Gio SE
~*~ i he = ee 8 % m i Sak es feats fiat Cn a5
=i ~~ a Eee s Lies 0 > : era eer Mi Mee Nee ee
. f > « - > %e " a Ya 4 <= x “ae
~ = 4 E - * Ps ie es ee awe NN > ae
; a Fats S Ea ae a tae
ys) Oe ieee to us THE CAMBRIAN. OO a
a us - : es f 2 ~e ~ c= J. » ‘a

—-

of a light gray color, in rarer varying from a fow a Bee to 2 or 3 ‘foot |

ness. It is formed largely of light gray, nearly white, compact, fine
grained, and massive bedded quartzite, with alternating beds of. hyaline |

were known to occur at a number of localities in Vermont, were found -
in 1887 for the first time in situ in the quartzite. The species belong” ,
to the genera Nothozoe, Hyolithes, and Olenellus. Traces of a trilo- —
bite, apparently of the genus Olenellus, were also found 100 feet above |
the gneiss on the western summit of Clarksburg Mountain. In the |
bowlders on the line of the outcrop of quartz, to the north of Benning- —
ton, traces of fossils have long been known, among which are Nothozoe |
vermontana, Hyolithes communis, and Olenellus thompsoni.

Prof. J. D. Dana describes the quartzite in its extension into western
Massachusetts, western Connecticut, and eastern New York. It varies

- very little from the characteristic nase shown’ at the north, and

from its disturbed condition no sections were obtained of its entire |
thickness. At Stissing Mountain, in Dutchess County, New York, ‘ite
rests upon the Archean, and is a massive bedded, compact quartxiGel
in which the genus Olenellus and Camerella minor nies ‘been found. - ‘It
here passes above into a limestone in which Hyolithellus micans, wehar- 7
acteristic Lower Cambrian species, occurs.+

In a paper read before the Geological Society of America at its | sec.
ond annual meeting, December. 30, 1890, Dr. J. E. Wolff gave an <a

Lower Cambrian age in the limestones of the East Rutland Valle 3
The limestones rest conformably upon the quartzite which carries

Kutorgina sp.? and Salterella. The evidence of the Lower Cambria
age of the limestones is not fully proved, as the two genera may range
up into the Middle Cambrian. | oa
He mentioned that in the West Rutland Valley, and in the valley
between the West Rutland and East Rutland Valleys, the limeston

be found above the Cambrian horizon. From his section it is probable
that the Middle. and Upper Cambrian faunas will be found to. a p
into the limestones beneath the Calciferous horizon, as has been di dit
covered by Prof. W. B. Dwight in Dutchess Cound: New Xork,

As a whole, the “Granular Quartz” may be said to consist of ashore
deposit accumulated along the western shore of the Green Mouontait

‘The Taconic system of Emmons and the use of the name Taconic in Geologic nomenclature, Ad a
Jour. Sci., 3d ser., vol. 35, 1888, p. 236.

2 Bull. Geol. Soc. Am., vol, 2, 1891, pp. 334, 335.

‘ f ~ _
W ae Se ag SS 4 . < - . _

& % 8 Ee"

4 md to mixtures of sand and argillaceous and calcareous mud.

: ~The“: Red Sandrock” series is confined almost entirely to northern
a ermont, not appearing south of Addison County. In the northern
part of Addison County it comes into contact with and merges into the
“ Granular Quartz ” series. It has not been recognized in contact with
28S of the character of a shore deposit and from its occurring west of
a deeper water accumulation, though contemporaneous with the “ Gran-
ular Quartz.” The Georgia slates, in the townof Georgia and in north-
erm Vermont, are conformably superjacent to the “Red Sandrock.”
3 S As the formation is traced to the south, the “ Red Sandrock” series
disappears, and the Georgia slates and shales. with their interbedded

limestones and sandstones, represent the entire Cambrian section; so
Bit i is very probable that the Georgia series as found in southern Ver-

ular Quartz” and the “Red Sandrock.” The “ Granular Quartz” has
been described separately, but it is more convenient to anite the ‘Red
# Sandrock ” and the Georgia slates, because the sections usually show
the latter resting conformably upon the “ Red Sandrock” series through-
Bont northern Vermont. The geographic distribution of the Canadian
_ extension of the “Red Sandrock” and the Georgia slates is shown on
_amap by Sir Wm. E. Logan, entitled “The distribution of the rocks
_ belonging to the Potsdam, Quebec, and Trenton groups of the east side

the Report of Progress of the Geological Survey of Canada for 1863,
z published 3 in 1865. The formations extend north of the boundary line
about 5 miles, where they appear to have been cut out by faults that
: P hring the superjacent formations into contact with them.

_ The “Red Sandrock” series consists of white and red dolomites and
; _ sandy layers. Some of the strata are mottled red and white, and a few
are brick red or Indian red. Some beds containa considerable amount
f siliceous sand, and all weather a yellowish or reddish brown. They
are also interbedded with gray argillaceous limestones and buff sandy

notes on the formation near the Canadian boundary. ‘To the south, in
_the town of Georgia, Franklin County, Vermont, they form a bluish
ay dolomitic limestone, followed by a steel-gray dolomitic limestone
th nat passes into a mottled limestone or the Winooski marble. This in-
turn is subjacent to gray dolomitic limestones in massive layers, some
of which are mottled reddish and white, though the larger part are gray |
and yellow. Still higher up the reddish pink dolomitie limestones ap-

pear. There are many variations in the color and composition of this —

>

hap the Canadian border and its point of Fpmfeera 40
miles to the south, :

Os SNA LEE, EE LE aaa te i leer Beta ent ea a BER
te " suMMARY—NoRTHERS APPALACHIAN. eee ye

Av as enety Cue tka. times; the sediments vary hows pure davis

x the Archean rocks of the Green Mountains. From this, and its having =~

t he line of outcrop of the “Granular Quartz,” it is quite probable it is -

om ont and eastern New York represents or is equivalent to the ‘ Gran-—

_ of Lake Champlain,” accompanying an Atlas of maps and sections of |

‘Se -dolomites weathering brown. This description is taken from Logan’s |

as . 4 re Poe ee "5 ae NR a ices > SO eee Ee ‘
he en % = oh 7 % ' “| ret f ~ he ; TP Peo oe t af Sed te
. et . kts a, 4 Pan a = .,
278 ae : THE CAMBRIAN. Be oui

- roofing slate; (3) clay slate approximating to micaceous sarldstones (4) >

‘rock ” and Georgia series, beginning at the base of the western face of.

ing southeastward to Parker’s quarry, a little south of the Georgia,

(A) Reddish pink, dolomitic limestone, weathering to a reddish brown and de-—

The Georgia slate series, pbeundin ¢ to Prof. C. H. Hitchcock, conan
in Vermont of several varieties of rock.! They are (1) clay. slate ; (2)

various kinds of limestone; (5) brecciated limestone ; (6) conglomerate |
formed of pebbles of limestone. ‘

A carefully measured section extending up through the “ Red Sand-_

the cliff overlooking the level that reaches to the shore of Lake Cham:
plain, in the town of Georgia, Franklin County, Vermont, and extend-

post-office, gives the following :?

Feet —

(1) Massive bedded, bluish gray dolomitic limestone, with many inosculating
threads and bunches of a yellowish-drab sandy limestone that weathers | .
Lin ROME? wi snag woes VES ue be saa cieckee Sa, Swe soba eee 33

(2) No.1 passes into a steel-gray dolomitic limestone that weathers to a dark ae
buff and bluish black, with angular fragments of bluish gray limestone —
appearing irregularly at the surface. At 160 feet from the base the first
band of mottled limestone, ‘‘ Calico” or Winooski marble, is met with.
The latter grades into a reddish dolomite, free from mottling, and then in ;
' a gray limestone. (Fossils, Hyolithellus?).............--..----...---- et

(3) Gray dolomitic limestone in massive layers, some of which are mottled,red-
dish and white, but the larger part are gray and yellow. Many of the
gray layers break up into a columnar structure, the columns being at
right angles to the bedding. In a reddish-colored limestone, 200 feet from
the base, a slender elongate tube occurs, probably Hyolithellus micans... 475 ~

i

composing on the exposed edges to an arenaceous, dark, brownish-red
rock that shows numerous fragments of fossils: Kutorgina labradorica,
Obolella (?) sp., Salterella pulchella (?), iyohoparte adamsi, Olenellus
EROMMOOWS 55 oh ele 56 cn sone dchn sas, ai grease hk Jen yo cantons saat nee 100 —
(5) Gray arenaceous limestone in rough, massive layers, passing into more .
evenly bedded, light gray, arenaceous limestone. Fossils similar to those
in 4 occur in the lower portion ........-...--- ha athe feted ete ana 190 |

Total thickness of limestone... o. 2c. 22nd ee See 1, 000 ;

(6) Georgia shales.—Argillaceo-micaceous and arenaceous shales, containing
numerous fossils, at Parker’s ledge, and showing deposition contact on |
Noor Sg cilas oe iw a Rah DOSE eg aac bakasn dadeene ak Saees ceeses* QOOu—E

Strike at Parker’s Quarry, N.30° E., dip 8° to 12° EB. a
The fossiliferous shales at Parker’s Quarry contain: Palwophycus in-
cipiens, P. congregatus, Diplograptus simplex [now, 1891, Phyllograptus (?)
cambrensis], Climacograptus (?)emmonsi, Kutorgina cingulata, Orthisina ori-
entalis, O. festinata, O. transversa, O. sp. (?), Microdiscus parkeri, Mesonacis
vermontana, Olenellus thompsoni, Olenoides marcoui, Bathynotus holupyga, ~~
Ptychoparia adamsi, P. vulcanus, Protypus hitchcocki, P. sencctus, and =
P. senectus var. parvulus,

1 Hypozoic and Paleozoic rocks. Report on the geology of Vermont, vol. 1, 1861, p. 358,

2 Walcott,C.D. Second contribution to the studies of the Cambrian faunas of North America. v.
S. Geol. Survey, Bull. No. 30, 1886, pp. 15, 17. ‘

3A mile south of the line of the section about 75 feet of arenaceous limestone occurs beneath > ‘hina
bed. Fifty feet from the base I found during the summer of 1890 Obolella crassa ?, Salterella sp. ?
Hyolithes 2sp.,and fragments of a species of Olenellus, A few feet higher in the section the heads of —
Protypus sp. ? and of Olenellus sp.? were found. Traces of the Olenellus fauna were also found - ss
85, 153, and 193 feet above the lowest horizon. +

; an
‘ * ~ ae -
“Se Sirs

ao oe iki as Sy eee oa a aly a a es 2g

~

oe Fee LL See ae Feet.
(7) East of the Parker quarry the Chen are jareillaceovs shales, with occasional
ea layers of hard gray limestone one- -half of an inch to 2 inches thick, that
carry numerous fragments of a linguloid shell.......-..-..---..-------. 3,500
____ Strike of shales near top of , N. 40° to 60° E., dip 60° SE.
(8) ‘Light RR A ako Al Sale pa tn nN pn btu tiene Wass bance s-nos oe 50
( 9) Gray limestone in massive layers, with occasional intercalated bands of
BS Ea hard argillaceous shale similar to that beneath the limestone. Many of
ie the beds of limestone appear to have been broken up into fragments and
recemen PMMA EPG RL EIN. ooh 2-00. co Cav oot ta awk Fhe o naga LN at 1, 700

Average strike of limestone beds N. 50° E., dip 50° to 90°; average dip
60° SE.
In this limestone belt, 1 mile north of where the section crossed, a few
fossils were found; Lingula, n.sp., Orthisina undt. (fragment), Camerella
‘undt. (probably new), Agnostus like A. orion, and Ptychopuaria like P.
adamsi.
x (10) Argillaceous shales, very similar to thoeét in the Parker ledge, continue on
up to the opposite side of the line of the Vermont Central Railroad track.
At the base the shales rest conformably against the limestone of 9, and
above appear to be eut off by a fault.
Strike N. 50° E., dip 50° to 80° SE., for a distance beyond the limestone ;
the dip then decreases and does not eeona 20° for a long distance, until
within 1,000 feet of the railroad track, where the shales become coarser
and changed by addition of arenaceous material, and the dip increases.
‘Total thickness to fault line of No. 10, 3,500 to 4,500 feet.

. No. 8 of the section when traced on its strike to the southwest increases in force
very rapidly to the thickness of 500 feet or more, and also changes from a quartzite to
‘amore or less calcareous sandstone, containing irregular fragments of argillaceous
shale. ‘Followed to the northeast, it soon disappears and the limestones rest directly
¢ n the shales. Continuing northeast on the limestone (9), it is found to decrease rap-
‘ic diy, and a mile northeast of where it is over 1,500 feet in thickness the width across

4

jogether, the limestone having disappeared. Southwest of the line of the section the
% width of the outerop narrows, and north of Georgia Plains post-office the entire
ection is covered by beds of sand.

No. 9 appears to be a great lenticular mass of limestone (lentile of Marcou) with
ntercalated beds of argillaceous shale, and more rarely with arenaceous beds imbedded
in the argillaceous shales. The fauna is Cambrian in character, and, in the absence
_ of Olenellus and other typical Middle [now Lower] Cambrian fossils approaches that
of the Upper Cambrian or Potsdam sandstone.

a section taken east of Highgate Springs beginning on the east
side of the same fault as the Georgia section, gives a slightly greater
t thickness, and more arenaceous matter in the limestone series beneath
the Georgia shales. The limestones are here 1,170 feet in thickness and
et the Georgia shales 1,000 feet, above which there is apparently a con-
_formable series of palearoons sandstones, with a thickness of 850 feet, to
where they are cut off by a fault line. A section measured east of the

village of Swanton, does not show as great a thickness of the limestone
» eneath the Georgia shale, and a fault line cuts obliquely across the
te b Bale. On the east side of the fault 200 or 300 feet of shales occur, and
many layers of conglomerate limestone, the fragments of limestone
rying in size from small pebbles to masses 6 feet in diameter. The

Va
w>
a.

=)
:

‘age "SUMMARY —NORIHERN APPALACIIIAN. ott Se eee eo

4 he outcrop is not over 150 feet, and soon the las above it and those below it come |

fossils in the Tigpabans con glomerate have an Upper Gandietan aspect, :

_ base is unknown, and it does not appear, so far as I know, i in the section | 4
_ between the poantlars of the United States and Canada and the out-

lent of the Olenellus asaphoides of the Washington County section or not.

oe es ree THE CAMBRIAN. Se ass tweet

leura. With the exception of the Solenopleura the species appear to be-

Jella, like Obolella crassa, Hyolithes americanus, H. communis, H. sp.
_ undt., Hyolithellus micans, and fragments of Olenellus occur. Inalead-

cp S. Geol. Suryv., Bull. No. 30, 1886, p. 19. 9 an

~

and inclade Lingula sp. ?, Agnostus sp.?, Amphion sp.?, Bathyurus sp. ?
Below the horizon of the conglomerate and in situ in the shales, tlieré’ |
were found the genera Lingulella, Agnostus, Ptychoparia and Solenop-

identical with those of the limestone lentile (9) of the Georgia section. —
A section measured east of Swanton by Sir William E. Logan gave but —
520 feet of the limestone (Red Sandrock) series! But farther to the —
north, nearly on the line of the Canadian boundary, he found. 1,410 feet
of lintestone in the section, proving that this portion of Caabriin ter-_ E
rane thickens rapidly to thenorth. — ;

The section measured in the town of Georgia is the most soniaioes yet
taken in Vermont (ante., pp. 278, 279). Atthe basea great belt of dolo-
mitic limestone 1,000 feet in thickness rests against, and, by an overthrust -
fault, overlaps the Trenton limestone of the Lower Silurian (Ordovician). —
What was originally beneath the Cambrian limestoneis yetundetermined. —
In the Highgate section the limestone belt is nearly 1,200 feet thick. The

crop in the town of Georgia. I have suggested that the great mass of —
shaly argillite east of the Vermont Central Railway track in the Georgia
section may be older than the limestone at the base of the section, bull |
until further evidence is obtained this is merely conjectural.”

During the field season of 1890 I studied the “ Red Sandrock” series
of the Georgia section, and found a little to the south and at the base ©
of the original section that there was a band of buff-colored calcareous
sandstone some 50 feet in thickness. In the upper beds of this, Obo-

ipioed: magnesian limestone, passing into a buff-colored limestone 14
feet above the sandstone, fragments of Olenellus and the head of Pty- |
choparia, apparently identical with P. trilineata, were found, and in the
superjacent pinkish magnesian limestone with interbedded adams: colored.
limestone, at horizons of 85 feet, 113 feet, and 198 feet above the sand- ©
stone, fragments of fossils that I recoded as portions of Olenellus and
very perfect specimens of Salterella sp.? occur in the decomposed sili-
cious limestones. oa
‘The discovery of the Olenellus fauna in the lower portion of this mag:
nesian limestone series gives the fauna a range through 1,000 feet ¢ 0!
limestone and the 250 feet of superjacent Georgia shale. :
The fragments and heads of the genus Olenellus that were found i in the
lower beds were not sufficient to determine whether it was the equiva-

' Geological Survey of Canada: Report of progress from its commencement to 1863. eal,
1863, p. 281. S “4
2Walcott,C.D.: Second contribution to the studies of the Cambrian Titinion of North 1

-

_

fossils. _As the vertical distribution of the fauna in the Olenellus zone
will be treated of in a future paper, farther reference will not be made
f a re ‘it at present. —

Lower Cambrian, but are the representative of the middle portion of
the ‘Cambrian section. This view was advanced by Prof. Jules Marcou,
in 1885,! except that he placed the same series of shales which occurs
at St. Albans beneath the Georgia slates or Olenellus zone. The stratig-
& raphy was erroneous, but the suggestion that the St. Albans slates cor-
respond to the Paradoxides belt of the Atlantic Coast area will proba-
bly be found to be correct. In such an event Professor Marcou’s name
«St. Albans will be a useful addition to the nomenclature of the Cam-
brian. group in northern Vermont. It will, however, be difficult to differ-
~entiate between the St. Albans group and the superjacent beds carryin g
s pee. Upper Cambrian fauna. °

_In the group of sections taken across New Hampshire and Vermont
= Prof. C. H. Hitchcock? the Georgia series is called Potsdam and

of gestion) are represented as resting dontoriably on the magnesian
limestone (Potsdam of section) in the town of Milton. This is the same
as in the Georgia section a few miles to the north. The great mass of
' argillites, east of the railroad track in the Georgia section, are placed
under the term Cambrian by Prof. Hitehcock, and the reference may
~ possibly be correct; but as yet there have not been any recognized
_ Cambrian fossils a in it, Ne: at this Ls or to the north or
south. : ..

In southern Vermont the Giahidis slate series widens out, and includes
- the great roofing- slate belt that extends through Rutland County and
into Washington County, New York. The outcrop of this series is nar-
y in the south part of Washington County, but it widens rapidly in
| Rensselaer County, occupying nearly the entire width of the county at
its southern boundary. At its greatest point of development in Wash-
ington County it consists of the following strata, as shown ip a section
crossing the county in the towns of Greenwich and Salem, with its base
1 4 miles west of North Greenwich post-office :

a) cong ciy layers of in:pure, ahaay limestone embedded in irregular argillaceo- Be
__ arenaceous shale, with numerous fossils of the Olenellus fauna in the
ES sa BE ia IL ale earn enh vB elnpsatis Sp v~ dans seme ns oa vam 340
_ (2) Massive layers of fine-grained, bluish gray, arenaceous limestone, that be-

-__—s come almost a pure limestone in places ........---..----- SL al oud sad ec 670

- About halfway of the mass Lingulella celata, Hyolithellus micans, and ~
__—-— Leperditia dermatoides occur. he

«
~>

ps The Taconic System and its position in stratigraphic geology. Am. Acad. Proc., vol. 20, 1885, table
f on n 1p. 224,
2 Geological sections across Vermont ate: New Disipiliane: Am. Mus. Nat. Hist., Bull., vol.1, 1884,

pl ‘tome

-

a .
. ot
wo

" SUMMARY—NORTHERY “APPALACHIAN, eee ley

bis: Paaite ath ee that it. Ais, from: the character of the associated —

a. The shales and slates superjacent to the Olenellus- pearing beds of |
the Georgia slate, at Parker’s quarry, do not apparently belong to the _

~ Cambrian ; and in section x1, on Pl. 17, the Georgia shales (Cambrian

rae ’ = PGS © ar tte r Serer ge Shy ba Seat te TRAE RS Con ge Teed ba
: - * ' PL he ing we Vals 4 * eos
Oe ot PIE Bb are See
282 - : THE PANES meee eccmews 2. >
> : ‘ ; -" a ; Feet. 3 .
3) Shaly limestone in massive layers; argillaceous chatea interbedded i in the >
ny Oi. SORES co. gS es caine Sim oes ae pean Speers Eth Rant ttn ea in Se aa ~~ * 200m

(A) Calcareous, argillaceous shales, in massive layers, with interbedded arena- —
aD. ceous limestones below, and passing into an argillaceous shale above... 240 —
8 (5) Dark, argillaceous, and arenaceous shales becoming fissile in places; occa- ::
-. .. gional layers of a hard, gritty limestone 1 or 2 inches thick occur at
various horizons. Near the summit of this section Hyolithes americanus,

. Microdiscus pulchellus, Olencllus asaphoides, and Conocoryphe trilineataoccur ~
near the roadside. This is the trilobite bed from which the original
, -specimens described by Dr. Emmons were obtained ....-.........--.---- 370
= on The section to this point gives a total of 2,600 feet, and is considered oa

Division A of the section.
(6) Compact, steel-gray, massive-bedded argillaceo-argillaceous shale » breaking x
bs into irregular fragments, and weathering a rust-brown color. .... oe wae 2 ae
At a point 1,300 feet up in this I found Stenotheca rugosa, Hyolithes amer- .
icanus, and fragments of Olenellus asaphoides. At 2,100 feet up fragments
of Olenellus occur in a stratum of calciferous shale. .
(7) Massive beds of a thinly banded, cherty, and argillaceous rock, capped by

. ry band of. calerferon® sandfock --.. .2.60-.i4 Ges eee ae, tee eee 400
(8) Argillaceous shale, more or less arenaceous and calcareous throughout-its
Oxtent 5. coogi hee edt cee ee Ge th Red enact ee ete ane 2, 400

(9) Calciferous sandrock, ‘light colored, weathering to a reddish brown, crum-
he bling sandy rock. This j is embedded in a caleareo-argillaceous rock, that
7 fests into angular fragments of a shaly character. The only fossils ob- _

served were Obolella crassa, Hyolithes, fragments uf Olenellus, on the — _

ia decomposed surfaces of the more calciferous layers....-.....---..------ 900
(10) Argillaceous and arenaceous shales, much like those of Nos. 8 and 9, with — y
bands of bluish gray, evenly bedded, and conglomerate limestone carry- a

ing fossils. As shown in the section, this division appears to have a thick-

ness of 4,500 feet ; but it is assumed that there is much repetition by_ ae
faulting, so that it is given a thickness of 2,250 feet............ Peet *, 250 7

The combined thickness of the section to this point is 10,750 feet. Its
continuity is here broken by a fault, that brings the rieke of the Hud- :
son (?) terrane against it and ean it and the purple and green slates
that form a large portion of the Cambrian section east of the rocks of ;
the Hudson (?) terrane. The section is again taken up on the east side —
of Salem Village, at the base of the green and purple slates and inter :
x bedded limestones, carrying characteristic Lower Cambrian fossils of

the Olenellus fauna. : a 4
Feet

(11) Green, purple, and higher up, gray wad dark shales and slates and inter-
bedded limestones, in very thin layers. ....-... 2-22 cene eens eee --ee eens Q, 500

(2) Nonfossiliferous green and purple slates ...-...----..----- ee eee een e eee 2, 150 |
In the township of Hampton to the north, the green and purple: slates a

appear to have a thickness of 4,300 feet; and 2 miles north of that point — a

there are over 5,000 feet of these beds, if no repetition occurs.

The luwer portion of this division is characterized by the Olenellus
fauna in association with some other species that indicate the Middle ae
Cambrian zone. The entire thickness of the lower and upper divisions, |. —

a according to the section, is 15,350 feet. 7a
(13) Above the green and purple slate belt is a series of greenish, schistose, i
hydro-mica slates, estimated to have a thickness of 3,700 feet. They are wel

not fossiliferous, and appear to pass beneath the limestones characterized | m

7 £:
a“ ' ey
e

we 3 ag eae me
“_ a wr

* § pie Oe.) ee eT ae ak tt ey eS eS a to at Dae re) ‘I 2S, . bed vo
=i wt 4 oe oe i 7, oe as Se ee | Le ate” . ad va. eo Se “
ey ; 3 x Po ee , , «
= ven . :

is ae Pt “SUMMARY —NORTHERN APPALACHIAN. owe.

by the o Chazy- Trenton Sues I have neleveud them to the Potsdam zone

Ps provisionally. 1 If this reference be correct and the rocks in the section |

si FE are not duplicated by faulting, the Cambrian system has a thickness of

s 19,000 feet in Washington County.

- This section may be greater than the actual thickness of the sedi-
om ents deposited in this region during Cambrian time. The upper 3,700
- feet of greenish, hydro-mica shales probably do not belong to the
(Cambrian, and there may be some reduplication in the section as meas-
ured. Eliminating the probable sources of error, I think there is at
_ the least from 10,000 to 12,000 feet of strata that may be referred to the
Cambrian group.

Se section 35 miles to the south, across the extension of this series,
xhibits a great development of the shaly portion similar to that in the
Bower part of the Washington County section, that passes above into
t the red and purple slate belt. In this section the upper member
of the Washington County section is apparently represented by a
¢ coarse, greenish sandstone, and in places a fine conglomerate. At the
base of this formation the red and green shales are interbedded with
the sandstone, the passage from the slates to the sandstone being by.
3 3 tercalation of sand and slate for a distance of several hundred feet, the
slate gradually diminishing in volume as the intercalation of the sand-
P “stone i increases. The sandstone is estimated to have a thickness of 2,000
feet or more, and it corresponds in stratigraphic position, and is on the
‘strike of the 3,700 feet of greenish hydro-mica schistose shales of the
“Washington County section. The recent work of Mr. T. Nelson Dale
roves this series (Berlin grit) to be of Lower Silurian (Ordovician) age,
q “and indicates that the series of green and purple slates beneath may
‘Ye resent the base of the Lower Silurian (Ordovician) and the summit of
the Cambrian.

Oe Our knowledge of the rocks of the Cambrian group in their southern
@ xtension into Dutchess County, New York, is obtained from the obser-
vations of Prof. Wm. B. Dwight. The base of the series is the “ Gran-
ular Quartz” of Stissing Mountain, that had been referred to the
Potsdam zone by Profs. W. W. Mather, J. D. Dana, and others. Occur-
ing between the gneiss of Stissing Mounthin and the superjacent lime-
a one carrying the Calciferous fauna, it was natural that this should be
ce elated with the Potsdam sandstone about the Adirondacks; and it
was not until the fall of 1886 that fossils of the Lower Oainbridt or
me enellus zone were found in the quartzite, and in the limestone resting
up on the quartzite.” Prior to this Prof. Dwight had discovered in the
& more or less arenaceous limestone and argillaceous shaly limestone
ar Poughkeepsie the presence of the Potsdam or Upper Cambrian

= Walcott, C.D.: The Taconic System of Emmons and the use of the name Taconic in geologic
nomenclature. Am. Jour. Sci., 3d ser., vol. 35, 1888, p. 241.
ere ht, W. B.: Primordial rocks of the Wappinger Valley limestones and associate strata,
Brothers Inst. Trans., vol. 4, 1887, pp. 206-214, Am, Jour. Sci., 3d ser., vol. 34, 1887, pp, 27-32.
=
= = 3 7%
..

PFS oa

JT fe

se Fat
‘bedded limestones, slates, and sandstones; and the limestone of t he

Saratoga County, New York. Sibsacenels he anodes in ove tee

_ that indicated the Middle Cambrian or Paradoxides zone. “The species
are Hyolithes billingsi?, Leperditia ebenina, Kutorgina StL and

the rocks are masked by the drift deposits. The succession as de eter
‘mined by the known stratigraphy, and the fauna is, first, at the base. a

the vicinity of Poughkeepsie the Upper Cambrian fauna occurs in a

replaced by slates, schists, and sandstones, both in Rensselaer a
_ Washington Counties. This difference in sedimentation is shown ¢

- to Cape Rosier. It represents the accumulation of sediments in a aa d-

that near the old shore line the basal sandstone, “Granular Quarta”

deposition, the lower portion of the limestones of Berkshire Count ts

- sedimentation of Middle and Lower Cambrian time. a’

fauna. . It ‘polugiad time acuminata, Obelella prima, Paha nab
-ealeifera, and P. saratogensis, BERS reese with those found at t 1

“stone above the quartzite, at the south end of Stissing Mountain, foss ils

— Olenoides stissingensis. -
The stratigraphic succession is more or ite interrupted by faults and t

massive bedded quartzite, restin ig upon the gneiss below, and subjac on
to a bed of hard, compact limestone. In the quartzite the Olenellus
fauna has been ioind and in the bed of limestone immediately su 2
jacent to it one of the characteristic fossils of the Lower Cambris
fauna, Hyolithellus micans occurs. In the superjacent limestone, the +
thickness of which could not well be determined but which appears rs
to be considerable, the Middle Cambrian fauna was found in an are-
naceous limestone, passing frequently into a caleareous shale ; and i in
somewhat similar limestone. : aa

The contrast of the sedimentation of this section with that of Wash-
ington County is very striking. In the latter, the quartzite of Stissing >
Mountain is represented by the great thickness of shales, and iute

Middle and Upper Cambrian of the Dutchess County section are entire

along the northern Appalachian Province from Dutchess County =
Canadian border, and on to Quebec and down the St. Lawrence River

ually sinking area and ina relatively shallow sea. It is a curious fa ot

of the Lower Cambrian is almost directly succeeded by the nate
limestones of the “Marble” belt. Unless there is here an area of ‘non-

Massachusetts, Rutland and Addison Counties, Vermont, represent th

-

The preceding paragraph was written several months prior. to the
discovery of Cambrian fossils in the limestones of the East Rutland a
Valley by Dr. Wolff, in 1890. (oie

~

1Discovery of fossiliferous Potsdam strata at Poughkeepsie, N.Y. Am. iAdians: Proc., vel 34, 18
pp. 204-209, ~
2 Recent explorations on the Wappinger Valley limestone of Dutchess County, New York, 5
discovery of fossiliferous Potsdam strata at Poughkeepsie, N. Y. Am,Jour. Sei., 3d_ ser, vol |, 31,
1886, pp. 125-133. Vassar Bro. Inst., Trans., vol. 4, 1887, pp. 1380-141, :

£6 bs w CANADIAN EXTENSION.

RY 3
ae - bay |

‘The Canadian extension of the northern Appalachian district i is from
e United States boundary northeast to the vicinity of Point Levis,
Fancbeo, on the western side of the extension of the Green Mountains,
or ‘ Sutton Mountain anticlinal, and from Quebec down the south shore
C ce ‘the St. Lawrence River to Cape Rosier, Gaspé. On the eastern side
‘the anticlinal the supposed Cambrian rocks of New Hampshire, cross-
| = the southeastern portion of the Province of Quebec to the Maine
boundary, are also included.
a The stratigraphic succession of the rocks referred to the Cambrian in
th e eastern Province of Quebec and down the St. Lawrence River to
_ Cape Rosier is not yet clearly determined, owing to the faulting, plica-
ti ey and absence of clearly defined Cambrian faunas in situ in the
rata. In the vicinity of Quebec, on the pica tae Be of Dr. R. Ww. Ells,
1e stratigraphic succession is as follows :!

P
th

eo
. af

bie (1) Black, green, and gray shales, with hard and heayy bands of grayish, some-
times yellowish white, quartzose sandstone, which are thickest in the lower portion,
s "and with occasional thin bands of limestone conglomerate, the pebbles being gener-
ally smal and the paste highly quartzose. The quartzites have occasional scattered
vebbles of grayish limestone. =~

ti nted shales, with bands of hard cota sandstone, generally fine-grained, and in
thickness from 1 inch to 1 foot, the massive quartzites being absent and many of
ae greenish layers being covered with fucoidal markings, well seen on the shore
above Cape Rouge and in the cutting along the road above that village.

— (3) Bright red shales, often with thin greenish or grayish bands, which in places
; “are ‘calcareous. The rocks on a smoothed surface have a striped red and green aspect;

n the upper part occasional beds of a foot or more of hard green-gray sandstone
occur,

u ilar, of greenish and grayish Sillery sandstone, ranging in thickness from 2 feet

- tone, which ranges from a fine-grained homogeneous rock to a fine quartz conglom-
rate, much of the rock being characterized by the presence of small flaky pieces of
‘ “A ale and scattered small pebbles or large grains of clear quartz, the bands of sand-
4 stone being separated by partings of various colored shale. The local and lenticular
‘character of the sandstone is well seen in the Sillery section, some of the heaviest
beds inland thinning out before reaching the shore in either direction. In the upper
part, at Sillery church, Oboleila pretiosa occurs, from which point an anticlinal
vex 08ses the river to Point Levis, and appears in the cliffs at the Victoria hotel, where
same Obolella is found.

| Peis the Upper Sillery Dr. Ells places the Levis shales and con-
- glomerates of Levis City, the shore extension below South Quebec and

Bt . Joseph and the west end of Orleans Island. In the Levis shales,
the eee roterate limestone, embedded in a calcareous matrix, carries

Sec ond Sarat on the gee of a portion of the Province of Quebec. Geol, Surv. Canada, new

(ae e we. “iF, : i
ae | SUMMARY—NORTHERN APPALACHIAN. he 285.

(2) Greenish, grayish, and blackish, with occasionally dark-reddish or purplish- .

4 (4) Red, greenish gray and black shales, with interstratified masses, often lentic-

upward, in which the Sillery quarries are located. This is the typical Sillery sand- |

A

~ On lithologie and stratigraphic evidence the line would be drawn at the —

- as consisting for the most part of hard quartzites interstratified with

“stone occurs in which the Olenellus or Lower Gambriag fauna, is ] pres-

_green shales in the Silurian (Ordovician), as I think they are above the

on the southeastern side of the axis, is locally made up of altered vol-

bo SE OS FI SS ae a Se ee eee ee eee
. ’ fe x a a ~ : ¥ ; Fale _ cae aot << -. = * fan
- b : <? ~ ae —<> 2
286 THE CAMBRIAN. . (> [BULL 81,
4 = ~*~

ent. The thickness of the strata referred to the Cambrian is not given
by Dr. Ells in his publication, but he told me that the measurements —
given by Mr. Logan were as nearly correct as could be determined.
These were 5,000 to 6,000 feet for the Sillery and Lauzon series. —

The little shell Obolella pretiosa ranges through from 1,500 to 2,000.
feet of the Upper Sillery ; and the lower or Olenellus fauna conglomer-
ate occurs in the lower portion of this range. | =

Dr. Ells refers the entire Sillery series to the Cambrian, and in this.
I mainly agree with him, except that the upper portion is evidently a
passage formation between the Cambrian and Silurian (Ordovician).

summit of the red shale; on paleontologic evidence, as furnished by the ©
Graptolites, I would include the upper portion of the Sillery red and —

typical Potsdam zone of America.’

The strata doubtfully referred to the Cambrian group babwedal Que.
bec and Cape Rosier, on the south shore of the St. Lawrence River, have —
already been described in the notice of the work of Mr. James Richard-
son, reported upon by him in 1870. (Ante., pp. 118, 119.) As they
may or may not beof Cambrian age, ne further description will be given.

The strata referred to the Cambrian on the western side of the Sut-
ton Mountain anticlinal, or the belt extending southeasterly from Que- |
bec to the Vermont boundary, are described by Drs. Selwyn and Ells”

mica-schists and black slates. All of this series, as described by them
js unconformably overlapped by the Sillery red slates, conglomerates, —
and sandstones. Limited outcrops of grayish subcrrstalline limestone s
are found occasionally in association with the black slates and quartz
ites. 3

The voleanie portion of the Cambrian, or group No. 2 of Dr. Selwyn?
presents a great variety of crystalline, suberystalline, aud altered rocks,
including “coarse, thick-bedded, feldspathic, chloritie, epidotic, and -
quartzose sandstones, red, gray, and greenish siliceous slates and argil-
lites, great masses of dioritic, epidotic and serpentinous breccias, and
agglomerates, diorites, dolorites, and amygdaloides, holding copper ore;
serpentines, felsites, and some fine-grained granitic and gneissic rocks,
also crystalline dolomites and calcites. Much of the division, especially

canic products, both intrusive and interstratified, the latter being clearly
of contemporaneous origin with the associated sandstones and slates.”
As far as known this zone has not afforded any fossils. Dr. Selwyn

! Walcott,C.D.: A review of Dr. R. W. Ells’s second report on the geology of a portion of the Prov-
ince of Quebec, with additional notes on the “Quebec group.” Am. Jour. Sci., 3d ser., brea 0,
p. 113. _

2 Report of observations on the stratigraphy of the Quebec group and the older crystalline r ocks of
Canada. Geol. Surv. Canada: Report of progress, 1877-1878, 1879, pp.5A,6A. » :

; oe | SUMMARY—NEW JERSEY. "et

ks that if found they would indicate a Sinthdcieen than the Levis
5 — tion, probably not far removed from the St. John group and At-
lant ¢ Coast series of Nova Scotia, or Lower Cambrian. Details of the
“lit hologie and stratigraphic features of the strata referred to the Cam-
Cad and their geographic distribution may be found in the reports

_ by Dr. Ells on the Eastern Townships of the Province of Quebec.

- "?
= -

- ‘s= o” SOUTHERN APPALACHIAN DISTRICT.

Pea Southern Appalachian District includes the outcrops of strata
- referred to formations of the Cambrian group in northern and central
3 New Jersey, southeastern and southern central Pennsylvania, western

Maryland, Virginia, and North Carolina, eastern Tennessee, northwest-
ern Georgia, and northeastern Alabama.

NEW JERSEY.

_ As far as known the rocks of New Jersey referred to the Cambrian
are found in the northern central portion as outcrops of a nonfossil-
‘iferous sandstone resting upon Archean gneiss and subjacent to a Mag-
_ nesian limestone that has been referred to the Calciferous zone of the
New York section. The greatest thickness assigned to it is 20 feet.

? peorely upon the lithologic characters of the sandstone and its strati-
graphic position. There is no positive evidence of its being the equiv-
ant of the Potsdam sandstone of New York. It may be Lower, Mid-
- Sain, or Upper Cambrian, and possibly of Calciferous age. From the
stratigraphic conditions to the north and south it will probably be
_ found to be of Lower Cambrian age, or the equivalent of the “Gran-
ular Quartz” of New York and Vermont. The lower portion of the
‘limestone series may be of Cambrian age, as in Dutchess County,
New York.
_ Among the papers presented to the Geological Society of America
at its second annual meeting, Decemver 31, 1890, was one by Prof.
frank L. Nason on “The post-Archean Age of the White limestones
of Sussex County, New Jersey,” in which he describes the discovery of
the Olenellus fauna in the lower Primal sandstone of Rogers that rests
-unconformably upon the pre-Cambrian rocks. He said also that fossils
-tObolella or Lingulella) extended up into the superjacent limestone.
Ss In Prof. Nason’s collection I recognized Qlenellus thompsoni, Obolella
or Lingulella sp.?, and the cast of a coral-iike organism that is prob-
bly a species of Ethmophyllam. These were found at Hardiston-
vil > and Franklin Furnace, Sussex County, New Jersey.

“A
—

otis ces is gating) af « pein of Gis Brovimss of Qhabee Geol. Surv. Canada, new
ies, vol. 3, 1889, pp. 1K-120K.
tay = 5 pation of Gon Ranburn Townships of Qoabes. Geol. Sarv. Canada, 1386,
mew "Ser. , Vol. 2, 1887, pp. 1J-70J,

The correlation with the Potsdam sandstone of New York is based

Pin. " ie
> ts pane a

op et ool a = ae Lt Fy, ee Ss ee ae, PE ge RS ne oe bh eR =a 4 a, te. 7 Sg
ee or es le AN RD ee atts BiB cc te og area) a ea
ue 2 - - be -- ») of * 4

s " = * A Le A S
- Sh icra ? _ c is. = = Pp J ~—rey =e ro par « ae JSTT ay on =. S
- = SE a Sr ee sok wea
~ ei he *7 tsi. 9S oe eee

SOG Tee “THE CAMBRIAN. TE Se see

DELAWARE. . Be eae ea !

The outcrop of the sandstone referred to the “ Potsdam * in ‘nates
western Delaware is very limited, and is noted only to indicate its
- occurrence within the limits of the State. ae
Date ’ PENNSYLVANIA. a

The rocks referred to the Ganbeked System in Pennsylvania by the -
latest authorities include the Primal quartzite of Prof. Rogers; and —
Prof. Lesley is inclined to consider the sandstone and slate of the South — 3
Mountain proper as of Cambrian age. The line of outcrop of the
quartzite extends along the boundaries of the various Archean areas —
from the Delaware River on the northeast, in Bucks, Lehigh, and ;,
Northampton Counties, southwesterly, with more or less interruption, —
across Berks, Montgomery, Chester, Lancaster, York, and Adams —
Counties, to the Maryland line. Prof. J. P. Lesley’s summary is as fol- —
lows:

a

The lowest Paleozoic formation in Pennsylvania, No: 1, logically identified with the —
Potsdam sandstone of northern New York, makes its appearance along the edges of 4
the limestone No. 2 at the north foot of the Azoic Mountain Range between Bethlehem
and Reading in Lehigh and Berks Counties; in Mulbaugh Hill, on the Lebanon —
County line; in Chicques [“ Chickis ” of Frazer] Ridge, on the Susquehanna, above —
- Columbia; *! the Welsh Mountain in northern Chester, and in the North Valley Hill, —
which stretches for 60 miles from the heart of Lancaster to the Bucks-Montgomery a
- county line north of the city of Philadelphia. _ Its only fossil as yet discovered isa —
Scolithus, but its position next beneath the Calciferous limestone is too well marked —
to admit of doubt. Formerly it entirely covered the mountain districts north and
south of the Schuylkill River, because it still spreads in sheets upon their sides, and —
in many places makes their summits, lying unconformably upon the gneiss. soa
The South Mountains proper, which separate Cumberland from York and Frank-
lin from Adams County, do not thus exhibit the fundamental gneiss covered. by -
a coating of Potsdam, but are composed of peculiar sandstone and slate strata sey-
eral thousand feet thick, which occupy the place of the Potsdam in the series, but can —
not certainly be identified with it. They may be considered the equivalents of the E
Ocoee and Sewanee strata of east Tennessee. * * * We may consider our South ~
Mountain rocks, therefore, those lying north of the turnpike fault, as of Cambrian
age.”
The sandstone referred to the Potsdam in Lehigh and Northampton
Counties is described by Mr. Frederick Prime, jr., as “a hard, compact
quartzite, of a yellowish color where weathered, and when freshly quar:
_ ried of a grayish tint. * * * The thickness, where it could be meas-
ured, was 21 feet.’” 3 ;
_ The quartzite varies in thickness from 20 to 300 feet, the ciate
thickness being in the “Chickis” section of Lancaster County, where,
according to Dr. Persifor Frazer, it reaches 300 feet. "Southwest of the

1 Chester, Freder ick D.: Preliminary notes on the geology of Delaware—Laurentian, Paleozoic, s nd 1
Cretaceous areas. Phil. Acad. Sci. Proc., vol. 36, for 1884, pp. 237-259. Wee.
2A geological hand atlas of the sixty-seven counties of Penusylyania, embodying the results of t hi *
field work of the survey from 1874 to 1884. Second Geol.Surv. Pa.,X, 1885, pp. xvi, xvii. __ fy
3Geolugy of Lehigh and Northampton Counties. Second Geol. Surv. Pa., D%, vol. 1, 1883, p. 205.

ri

to its disturbed condition. The characters of the sandstone appear to
be very much alike throughout the State,and the only traces of organic
peapoine found are the straight, vertical tubes of Scolithus.

Prof. H. D. Rogers referred a series of slates, between the sandstone,

period, butthe Snidiiats of the Second Geological Survey consider them
keimzing to the limestone series. If a comparison be made with the

K au nd the limestone are characterized by Cambrian fossils, this series of
s schists will certainly be referred to the Cambrian, as it is subjacent to
the great limestone series and superjacent to the quartzite. According
to Prof. Rogers, the highest or Primal newer slate is a greenish and

as a thickness of about 700 feet. Dr. Frazer refers about 1,600 feet of
“Hydromica schist” to the interval between the quartzite and lime-
stone in York County.!

q The upper part of the Primal slates does not appear to be developed to
tl 1e northeastward in Lehigh, Northampton, Bucks, Montgomery, Berks,
and Chester Counties. It first appears with any considerable thickness
‘in Lancaster County, near the Susquehanna River, and south of the
-quartzites of the Chickis Hills. From thence it extends southwesterly,

4 hickness in Maryland and Virginia. ~
; ‘i Asa whole, the Cambrian System in Pennsylvania appears to be rep-
‘resented by the lower quartzite and the superjacent shales and schists
as originally defined by Prof. Rogers, and it may be that the lower
portion of the superjacent limestone will be included.

Ina letter received from Prof. Lesley, dated May 8, 1890, he says:

4 Reading Ells’s paper and Brainerd & Seely’s paper in Bull. Geol. Soc. America, just
‘pr blished, with your remarks at the mecting, I naturally reverted to my South Moun-
tain surveys (20 years ago) east of Pham bersbarek Pennsylvania (Fulton and Adams
¢ counties), and the strange and powerful impression made on me then by the outcrop
a low ridge of purple shales, running from the pike southward, just back (east) of the
4 peters mountain ridge. I never saw anything like them, and feel strongly in-
cline 1 to consider them the Sillery purple shales (Cambrian) of the North. I can’t
find or remember any description of this outcrop by Erieer. It liesin Fulton County,
outside the Adams County line. 4;

a : MARYLAND,

Ss have been auahic to find any detailed Sannin’ of the rocks referred
to the Primal series of Prof. Rogers, and have depended upon the gen-
al account given. by Prof. P. T. Tyson in 1860, in his report as State
: ae chemist. His description is short and will be quoted in

i imal of Pennsylvania survey.)—Potsdam of New York.—This division includes :
. ® ‘A hard sandstone made up of grains of quartz, with occasionally grains of

5, P. 401.

_ Bull. 81——-19
ee. aces

Ae

, -

Fealled Potsdam, and the base of the superjacent limestone to the Primal.

EA Tennessee sections, where the schists and shales between the quartzite _

‘Diuish talcose argillaceous slate, sometimes very soft and shaly, and ~

across York and Adams Counties, to the Maryland line, increasing in—

e oneral notes.—Sketch on the /eeology of York Speers: Pennsylvania. Am. Phil, Soe. Proe., vol |

al Pt

a0 cle

abe and kaolin. The siliceons coment seems to have sceiibeis ‘filled up tl
_ interstices between the grains so as to give a firm compact structure to the tock.

New York and Pennsylvania, but I have not as yet been able to oe reliable in

_ is probable that the extension into Maryland is the same. —

_ jight gray sandstone, in some places containing beds of a rather coz

instances, a brownish slaty sandstone occurs, alternating with the fo fo
mer, whilst toward the top or approaching the next formation the be an

‘slates. As far as known to him in his earlier work the formation om i

Be “g-

-

Portions of this rock seem to have been subjected to such changes as to render i :
doubtful whether it should not be considered a granular quartz and be classed among
the metamorphic rocks. Vegetable life seems to have commenced at the porketn of
the formation of this rock, because it contains fossilized stems of plants.

(2) A slate varying in color from gray to brownish and greenish. It is reniaal
an argillite, but portions of it assume a marked talcose appearance, especially in bh >
Catoctin Mountain and in parts of Middletown Valley, where it has been much dis-
turbed and altered by proximity to intrusive rocks. These last consist of amphibo-
lites (trap), porphyries, amygdaloid, serpentine, and epidote. This last-named rock is
extensively developed both in large masses and intercalated between the slates, an 1
has largely contributed to produce the highly fertile soils of Middletown Valley. y

Approximate measurements of the thickness of these strata have been made in

formation upon this point in our State.’ 5

From this description and the geographic distribution of the Primal
series as indicated on the accompanying map, it is evident that _ :
quartzite of South Mountain, Pennsylvania, extends nearly north ¢
south, across Maryland, and that the slates and associated rupli
rocks which form the main mass of South Mountain are included 9
Prof. Tyson in the Primal series. In the sections of these slates 2
accompanying rocks in Virginia they are recognized as pre- Combrisal
and it is very probable that those of Maryland and north into South
Mountain of Pennsylvania are also of pre-Cambrian age. The pres
énce of the upper Primal slate of Rogers between the quartzite and thi
Auroral limestone is not noted by Prof. Tyson. The fossilized stems 0
plants referred to are probably the Scolithus borings found so abun
dantly in the sandrock of Pennsylvania and Virginia. If the lowe
portion of the limestone series of Pennsylvania is of Cambrian agei

4

VIRGINIA.

Prof. William B. Rogers’s description of the geographic distribu ion
stratigraphic position, and character of the strata that he referred to t
Primal series, has been proved to be in a large measure essentially ¢ 201
rect by the observations of geologists who have more recently studie
the formations referred to the Cambrian group. He described form:
tion No. 1 as consisting in the most part of a close-grained white §

conglomerate of white siliceous pebbles. Near the bottom, in ma

stone passes into reddish and brownish and olive-colored argillas
Virginia was exclusively confined to the western slope of the Blt
Ridge and the narrow belt of rugged hills and mountains exten ndit

1 Tyson, Phillip T.: First report of the State asricultural chemist of Maryland. al
PP. 34, 35. :

291
| nenee ce to the Sinihenccmcnt of the Valley limestone.! At some later
Ge iteraver, he discovered a small eutcrop of the Primal series on
a destern: slope of the Blue Ridge, in Rockbridge County, and drew

it bin ou section 9 of the plates of sections published in connection with
The Virginias” in 1881. The Primal sandstones and shales are rep-

_ Archean rocks of the Blue Ridge. In this beautiful series of illustra-

Fiances from the Potomac River to the Tennessee line illustrate very

er, and thickuess of strata forming th? Primal series.
Prof. W.M. Fontaine in 1875 supplemented the work of Prof. Rogers

z ; alcony Falls i in Rockbridge County, Rockfish Gap in Augusta County,
z id at Harper’s Ferry on the Potomac. He concludes that the entire
Pt nickness of the Primordial strata at Harper’s Ferry can not be much
S over 1,000 feet, and that they are composed of slaty rocks, similar to

» variety of the lowest slate seen at Rockfish Gap, and a sandstone

same locality. The section differs from that of Rockfish Gap and Bal-
_ cony Falls in the absence of the coarser materials and the succession

x of shales and sandstones, with the subjacent conglomerate that rest on
the Archean. The lower argillites, forming the main portion of the

Yo. 2 accompanying “ The Virginias,” Prof. Fontaine refers to the
tea ; whether of Laurentian or Huronian age, he does not under-
take to decide.” :

- At the second annual meeting of the Geological Society of America,
at Washington, D. U., December 31, 1890, a paper was read by Messrs.
a 8, Geiger and Arthur Keith on the structure of the Blue Ridge
,ear Harper’s Ferry.

E savenal sections, taken on both the north and south sides of the
col Potomac River, show that the geologic succession at the base is a

which corresponds to the Medina sandstone of the sections farther to
‘the north and south. This section is the one described by Prof. Rogers
y s an overturned section, the quartzite corresponding to the primal
“quartzite of the Pennsylvania section, its present position being
ace inted for by the complete overturning, thus reversing the section.
The
rmal one from the pre-Paleozoic rocks through the limestone and

ppd, 1838, pp. 14, 15.
eology of the Virginias, 1884, pp. 167-169.
_ Rey eport of the progress of the geological survey of Virginia for 1838 (Richmond, 1839) pp. 6, 9-12,
Geolog, wy of the Virginias, N. Y.. 1884, pp. 197, 198, 203-209.
0 m the Primordial strata of Virginia Am. Jour. Sci., 3d ser., vol. 9, 1875, p. 425, —
= * 5

f :
es >

= ar
, az
i “e

= a.

‘res ented as occupying a varrow, deep basin on the eastern slope of the

ions the twenty sections crossing the Primal series at subequal dis-

mestone upon which rests a series of shales, subjacent to a quartzite _

authors of the paper mentioned conclude that the succession is a

= of the progress of the gelogical survey of the State of Virginia for the year 1837. ©

‘fully Prof. Rogers’s interpretation of the geological structure, charac-

Db 2 detailed description of the secticus of the “ Primordial” strata at _

“which much resembles some of the quartzites of the lower strata of the —

Feige and which Prof. Rogers included in his Primal series in section

“€ —j i rege Y i %
ay te 2 ag ah:
, + . : 7 eee - uN ee a “A w ie
Bikes te pes : a (REE ee
oo : > “ie % 4” ar? Ee fo
5 / ; Py aah uae , Sah. OT ee eee
. > ea se mein #

. shale to the sandstone. “The basal limestone is of + Caleiferous—Chazy- :
Trenton age; the shales then would correspond to the Lorraine series, —
and the sandstone to the Medina series of the New York section. As
as far known this is the only break in the continuity of the outcrops —

of the ‘Granular Quartz,” where a quartzite is presenty: from central ©
Vermont to Alabama. ! —

At Rockfish Gap the massive chloritic argillites, that form the mass

of the Blue Ridge, are shown in unconformable contact with the lowest
Primordial strata. The Archean argillites are firmand hard, of a dark
greenish color, and present a strong contrast to the first stratum of the .
Primordial rocks, the line _of junction being strongly defined. Sum-
marized, Prof. Fontaine’s description of the section is as follows, begin.

- ning at the base:? |

Feet.
(1) Very thinly laminated slates or shales -. 2.22. 2... 222. cee cee oe cee cece we nene 300
(2) On the side next to (1), the layers of this rock in color, do not differmuch
from (1), but are thicker than the preceding slates, and moresandy. The |
bedding thickens, and the amount of siliceous matter increases to the
west, until a fine-grained white kaolin sandstone is the result ..........
(3) Conglomerate of brownish-red color, in massive layers from 5 to 6 feet.
thick, with thin seams of shaly matter between several of the layers. .
The coarser materials are rounded grains of quartz of the size of a garden _
. peaand under; inclosures of angular fragments of the slates of the Blue
Ridge are NOt Tare .-- 22. 22-2 ne cee cence cee ce wowed soc nee ese cen coccen
(4) This is a partially concealed interval of 200 feet in which the rocks are,
when seen, kaolin shales and kaolin sandstone, principally the former. —
To the west of this is a band of kaolin sandstone, with layers of cellular, —
much indurated quartzite, and some subordinate beds of an indurated,
gray, coarse sandstone. This series contains one bed of the gray sand-
stone 20 feet thick. Thickness 420 feet or including the partly con- PS
eenlod band s2s..) eiccep wns nan Sp emec en ser cpee Sect eee eee ee 620
ey rg 3) The first rock in this series is a highly ‘idizoabed gray sandstone, the type.
ee of the beds above mentioned as forming occasional layers in No. (4). It
is of a dark gray color, and composed of coarse grains which by meta-
morphic action are changed to a nearly compact texture. The thick-
ness of the sandstone is 50 feet. A band of diorite 20 feet thick inter-
rupts the section, next to which is a band of bluish gray, coarse shales, ce
75 feet wide; a partially concealed interval of 300 feet, occupied by
similar rocks; then for 200 feet, several alternations of the same shales
re with bluish argillaceous sandstones. In these a layer 6 feet wide of red
_» argillaceous hematite is found. Then a second band of diorite 12 feet’ —
, wide, resembling in all respects the first.

(6) The beds of No. (5) which are mostly sandy shales, and are rather thickly-
bedded in layers of from 1 to several feet, are succeeded by a band of —
very thinly-laminated, firm olive slates or shales, having a total thick-

SHOE OL. ocs5 ito en ews one's neeh Ace p eee ee ae Me eee ania oe aioe ae ae
Indurated brown sandstone, with some chlouite........-...---.---- acxaaibs ‘
Suterval'of concealed rook. >... ~ «x. 22.Soscc aan one ec eben atu en eee
Alternations of brownish argillaceous san dstones with greenish shaly beds.

Se Very finely fissile, pink-colored slaty shales, which weather ag tersc lig 20
Then for 100 feet a bluish shale is found ....-...-......2...-------- Spree 10

-

1Bull. Geol. Soc. Am., vol. 2, 1991, pp. 155-163. | 2Am.Jour.Sci., 3d ser, 1 VO). 9 1875, po. 6- 2

a> ‘The two last | series of beds, 5 and 6, appear to be the equivalent of No.
© (8): of the Balcony Falls section. Their combined thickness is about 1,450
feet, that is, provided no reduplication from folding occurs. This is
possible, though not probable, I think.

stone, and resemble No. (10) at Balcony Falls in their almost total free-
dom from iron and other coloring matters. * * * The system here
consists of a vast number of thin layers, in which we may distinguish
three classes of rock: (a) A shale pale gray to bluish gray when fresh,
ie composed almost entirely of kaolin, and occurring in thin plates. (6)
This is associated with a very fine grained kaolin sandstone, the quartz
er grains being now perceptible to the naked eye. * * * (c) A kaolin
sandstone of moderately fine grain, often with a thickness of several _
“S feet in the individual layers. The quartz grains are mixed with an equal

Ss
~

- “The beds last described have a thickness of 300 feet, Fes are suc-
ce eded by a partially concealed interval, in which 50 feet of a similar

tone are largely concealed.
‘The one as studied at Balcony Falls by Prof. Fontaine is as s fol-

eS t ; Feet
(1) Unbedded quartzite, with crystals of feldspar....... McC usisi come ees 120
(2) Brown, crumbling, argillaceous rocks or sandy shale, conglomerate in its
I Ti | 25 noo. 5 his vos waebak wae gd ve anndectsse. wes 40
( (3) Brown, decomposing, thinly laminated and contorted shale............--. 10
(4) Conglomerate, like the upper portion of rts toe odin ke ade edn oss 20
© ae SS Se ae Ol Chena waa wae ooh dude Ueacetee 12
(6) Conglomerate, like (4)..........-- OE ee Pee Me a Pee itr £ Suge 15
7) Crumbling, brownish shales, passing in the upper portion into argillaceous
oa sandstones of the same hue and texture..-.........--22 .2-ee seneee eee 200
®) Massively bedded, coarse white quartzite (apparently Rogers’s typical 7
ES CE ge ea ee ener ee Peon Pere bar 500

F __-Up to this point the rocks are well exposed in the cliffs which closely
border the canal. Proceeding west across the strike, we next encoun-
___ ter a series that forms No. (9). .
(9) Thinly laminated, gray and reddish shales. Probable thickness..-....... 600
a f0) Alternating beds of quartzite and kaolin shales. Probable thickness.... 700
7). The first rock seen next to the mountain is thinly laminated, fragile shale,
of yellowish and reddish hues not fully exposed. Next, to the west, we
have bluish calcareous slate, and slaty limestone, 50 feet. Then very
_ thinly laminated, firm, deep red slates, 60 feet. Next a similar slate of
blue color, 15 feet. Then a bed of dark blue, hard, and dense limestone,
used for cement, 13 feet. Then thinly laminated red slates, 20 feet.
Then coarser and thicker bedded blue slates, 40 feet. Lastly, a coarse,

2, 455

He compares the Balcony Falls section with that of Rockfish Gap,
‘ing that the thickness of Nos. 5 and 6 in the latter section is much
r than that estimated for their equivalent, No. 9 in the eee

1Am. Jour. Bek; 3d ser., vol. 9, 1875, pp. 363-365.

- MIEN Sel Ro Cas wn aa maw woth cote Sacesacs se f ip maak 300°

rock are shown.” The strata between this point and the Auroral lime- |

rough, massive, siliceous limestone, 40 feet .......-.-.-----2.--+2-0-- s- 238

sy > > “- ~ — an © hate e ee a oF oo >s
beta arg es B ae “. a Se eS es age ' Spy. By ae 2 ke Pats aay os
~ ‘ - - 4 _ ARES _ ~ oy: a. “Fy wae ‘ ark + = ze Aaa ay a Ps SAE * 2 ro
7 7 é uf : ot ° mee 4 , a -_ ere - oa i a 2. ‘ = “ty j a g
294 ~~ fd 2c ~ .* Ww? 2 oe. + > fe 4 ee ce eae oe
— at a eeA ‘THE CAMBRIAN. ee
- ‘ ~ ie . 2 ~~ : bak eS 5;

S Falls meotiog: showing that the orapdaeia a shaly matter in dis. entire :

he Says : | | 4 F

Beginning with the base of the Spare gira he recognized six divisions | :

the places where the junction of the Primordial with the Azoic is exposed. * * *

‘we may be sure that we have the true base of the Primordial. I have never seen it

- Virginias, vol. eee pp. 22, 42-44, ae .. aaa

a

~

group at Rockfish Gap has greatly increased.! hk
In summing up the physical characters of the sections as deserted, ¥

It will be seen from the above notes beats in Virginia we have below the calciferous
limestones a great development of sandstones, shales, and conglomerates, | which —
attain in the middle portion of the State a thickness of over 2,000 feet, and i increase — 4
in the proportion of coarse materials to the southwest. They probably attain greater —
thickness in that quarter, while to the northeast the amount of sediment diminishes, —
and the proportion of tine matter increases. This change is plainly due to the —
increasing development to the southwest of the syenitic rocks which formed the shores “
of the ancient seas and to the greater violence in that direction of disturbing forces. —
The Potsdam sandstone forms one of the upper members of this group. Much further ;
study of these strata is required to settle the question whether the entire series is a —
great expansion of the Potsdam or whether divisions may be made corresponding to_
other epochs. The fact that at Rockfish Gap, and to the southwest, a great body of —
ferruginous slaty shales separates the lower highly siliceous and altered, sandstones _
from the upper Kaolin sandstones of probable Potsdam age, seems to judicata a change
in the conditions of sedimentation sufficient to justify such a division, in which the
‘Acadian strata may be found.? mo

With the single exception of a Scolithus, no fossils have been found — ;
in these rocks which would indicate their age. | SS

_ In 1883 Prof. Fontaine supplemented his detailed ticaakivilae of the
sections by a synoptic description, embracing the general character of fa

all the formations that he considered belonging to the Primordial series.? |

as follows: eS

Feet.
1. Lower Primordial conglomerate. .........-.....--...---- 0 to 30
2. Lower gray shales and flags......... Sai oe: sotoe np ates mere 500
3,. Red sliales ‘and flags... 35. 4.2025 100d odes cael le “wees 400
4. Upper gray shales and flags...........-.-. petcepeas kee om ee:
5. Potsdam quartzite........-... emi diene deine talem 350°
6. Ferriferous shales .............--. panes wintinas teeta apn Tes 500
~ 2,380
The decertntin of the various formations i is so aiear and fall. that I
quote them : | ; a

(1) Lower Primordial conglomerate.—I would confine this appellation to ae lowest
conglomerate that forms the base of the Primordial where it is present, excluding the 2
conglomerate bands that follow higher up, but are separated from the basal conglom-
erate by shale and slate. * * * This member, thus limited, I have not seen at all

~The conglomerate now in question is of special importance, since, when it is found 1,

without finding the Azoic rocks immediately under it. It consists of a finer matrix
that is shaly or slaty in texture, in which particles, angular or rounded in shaj De,
of the Azoic strata are imbedded. The lithological character of the pebbles varies

1 Op. cit., p. 421. . 2 an
2Op. cit., p. 424. é ~
3 Notes ou the mineral deposits at certain localities on the western part of the Blue Ridge. The

Res Soe or sec
SE Be oe 3 5 eed

a aa ; “SUMMARY —VIRGINIA. Es eae 295

in the more Sisetheriy. portions of the pelt a good deal of partly decayed feldspar
‘me ay be detected in the finer matrix, but to the horth argillaceous material forms
= » cementing matter (p. 22). |

0?) Lower Gray Shales and Flags.—The lower portion of this member of the Primor-

purplish in color, imbedded in a fine-grained watrix of shale or slate * * *
ba y . 42). ty, -

~The lower gray shales and flags vary in character more than any other member of
he Primordial. The predominant rocks are shales, that sometimes become slaty in
irmness and thinness of lamination, or various more siliceous flaggy rocks that range
f om purely argillaceous shales, through argillaceous sandstones, into massive and ,

UR
‘ors
vi

predominant color is gray, but reddish, yellowish, or purplish and greenish colors
‘801 ometimes occur.

; - Some of the grayish white, a argillaceous strata form a species of claystoune that
weathers to a sort of kaolin. For the sake of distinction these may be called kaolin
flags. This kind of rock is much more common in the member next under the Pots-
es quartzite. The conglomerates occurring in the lower part of this member have
en already described.

“The general features of the quartzite members of this group have been already suf-
fi iisientiy discussed. Towards the southern portion of the belt, they attain great dimen-
si ons. This is especially true of the space between tho southern border of Augusta
enaty and Balcony Falls. At this latter place a quartzite formation oceurs about
150 feet above the base of the Primordial, forming the Balcony Rock. It lies in huge
beds of a highly siliceous character, and is not less than 250 feet thick. Here the
massive character of the beds has prevented the cracking and smashing, accompanied
y ith the infiltration of silica, so often seen in the smaller beds of quartzite at this
ee in other places; otherwise the character is as given above for the lower
3 4q egone I have never seen any casts of Scolithus borings in these quartzites. The

x f the belt, its place being taken. by minor beds of quartzite, and by shales and flags.
s subdivision of the Primordial beds now being described forms the lower portion
“of the Primal older slates of the brothers Rogers.
‘. <4 (3) Red Shales and Flags.—This alsg is quite a variable group, and it chan ges its
= character very materially as we go south. In the northern portion of the belt, as far
Ee atacnit Torrey, the greater portion of this group is composed of a fine-grained,
very thinly laminated, and tender slate. When fresh this rock has a steel gray color
ged pearly or nacreous luster, but on weathering many portions become deep blood
ed in color. Some of the lower and upper portions become yelluw, but red is the
ee predominant color from weathering. Some bands have small pebbles of the size of
ob Dird shot graduating into sand. Some of the red and yellow colors may be original
and not due to weathering. This can not be decided, as all the exposures seen were

m such weathered. This member, in its northern exposures, is often affected by faults
‘that cause it to extend over greater breadths than it could occupy in virtue of its
Sith ts, Quartz veins occur in it, having the nature of fissure veins. Bands of
his slate are impregnated with more or less specular iron, and this is the highest
mber of the Primordial that shows iron in the specular form. Some greenish,
| ich indurated quartzite occurs in this member. This group to the south becomes
: ag ore siliceous and the amount of red coloring matter diminished.

nn Big Mary Creek the slaty character is nearly lost and the amount of red matter

‘i much less. The strata are now chiefly rather siliceous gray flags, and this charac-
ter is. maintained to Bercing Falls; there a rocks at this horizon are pies all

Be

=

th
ae
a
7

di: frequently contains bands of conglomerate, composed of quartz pebbles, often —

i ighly_ siliceous quartzites. These latter have the character described above. The

reat quartzite at Balcony Falls disappears almost entirely in the northern portion ,

=

-

gt a alin Sed eR eer FOS Eine lal Mo ee Pa he Shag Ut re Pe Seyi ee
{ “ j t < . y 44 5 2 Sia =
“ ; e~¥ a ha tS y < 4 i. es
9 ee

¥ we 7a —_ es, a =¥ at atte
Tbe sae ne eat CO 5S OR EG ORR eam
EF ‘ ree ~ oat ne 7 a Sgaray ais at “pa
2 DOGe5) Ae ee “THE CAMBRIAN. Ley? Gy Be Fe8 bach
- ' y Seow oP SOR A Oe a

flaggy and ; gray in ee. some va ¥eulabals and brownish bai ioneue Fae TE ‘This
change to a more siliceous nature is accompanied by a great increase in the accom-— ‘of
_panying quartzites. These strata everywhere, owing to their comparatively greater.
capacity for yielding to strains, have suffered much from contortions and minor ee a
faults. re
_ (4) Upper Gray Shales and Flags.—This group, as the name implies, is. bien iaie
like No.2, but in it the conglomerates and specular ledges are wanting and the — =
amount of quartzite is usually much less, Owing to the brittleness of the material
_ of the beds and the ease with which many of them yield to crushing, portions of the
strata are often found crushed to loose fragments. In the fractured and crushed por- —
tions important deposits of limonite are sometimes found that are evidently produced
by the concentrating action of percolating waters. The reddish and brownish rocks
found in No. 2 are also wanting here. The predominant rocks are shales and flags,
usually all highly argillaceous, and when fresh of a gray or greenish gray color, but
_ on weathering apt to assume a grayish white color. Towards the top quartzite ledges__
are interstratified with these and cause a gradual passage into the Potsdam quartz- —
ite. In some places the amount of quartzite here is very large and should properly —
be counted as a portion of the Potsdam member of the Primordial. Perhaps the pre- _
dominant rock is a gray shale that resembles a hardened mudstone and which grad-~ —
_ uates into a sandy shale. This rock often decays to a pure white clay, and nodoubt
furnishes the material for the pure potter’s clay sometimes found immediately west —
of the Blue Ridge. These strata for the sake of distinction may be called kaolin ay
shales or flags. . 7
(5) Potsdam Quartzite—The members of the Primordial below this, so far as ob- —
served by us, show no indications of the former existence of life. This portion of the ——
formation, however, shows in some beds numerous casts of Scolithus borings, some
_ of whick are remarkably long, being visible for at least 3 feet. The brothers Rogers nt
considered this member as identical with the Potsdam sandstone of New York: This —
portion of the Primordial is more constant in lithological character than the subdi-
visions that underlie it. Quartzite is always the predominant rock in it, the romaine a
ing portions Leing mostly composed of the kaolin shales and flags. To the south,
and especially in the interval from Mount Torrey to Buena Vista furnace, the quartz-_ -%
ite is very massive and siliceous, composing nearly all of the rock at this horizon. =
_ The material is more properly called a quarfzite than a sandstone. The upperand ~
lower portions are often flaggy, and cause a passage into the. underlying and overly- —
. ing shales and flays. So far as observed, these quartzites are never conglomeratic, —
and they are free from the infiltrations of silica, the diffused chlorite, and other char- a 3
_acters that mark the lower quartzites. Near the junction of this member with No. om
4, the strata are often crushed, the crushed band holding important deposits of a ‘ ‘
nark limonite. The Quartzite members of this subdivision are sometimes broken up
and crushed, forming a curious band of breccia, cemented by iron or manganese.
Sometimes workable deposits of limonite are found in these disturbed portions. J
(6) Ferriferous shales.—It might bea question whether these shales ought not rather — .
‘to be counted with the Calciferous group. It is certain that there seems to be a :
gradual passage from the shales into the pure Magnesian and Siliceous limestones, —
_ that correspond to the Calciferous sandstones of New York. No fossils are found to 4
settle the matter, and it seems best to draw the dividing line at the first marked bas
change in the lithological character of the strata. This change occurs with the low- zy
est limestone beds, that usually occur interstratified with reddish and yellowish 5
shales. :
_ The Ferriferous shale group is noteworthy for containing throughout it deposits of
imonite which are often suited for the manufacture of a neutral iron. These depos- —
its seem to be of concretionary origin, formed by the decay of the shales which con- |
tain the iron in a diffused form, probably, for the most part, as a carbonate, but
-sometimes as pyrite. These ores are consequently usually imbedded in clay. They ea

. . 5 .

2 5

Bah ok " SUMMARY—viRGINIA. pene ete a ea,

’ s the form of lenticular masses, tihanliy built up of concretionary forms. These
are unlike those found in and under the Potsdam sandstone, and not rarely are
: sled with oxide of manganese or associated with it, forming ferro-manganese. In
manner, we find, not rarely, deposits of quite pure manganese oxide. This is always
ie in the form of Psilomelane or hard manganese.
_ The lowest of the strata of this group have the character of kaolin shales and
flags. They graduate insensibly into the Potsdam quartzite member. In ascending
- y become purely argillaceous shales, generally of lead, or bluish gray color, when
il With these, moreover, occur strata yellowish-reddish in color, the red often
“as uming a pinkish shade. Towards the top, ledges of pretty firm pure purplish
‘shales and flags are found that are sometimes of the nature of fine-grained sandstone.
I ‘The shales towards the top are often calcareous, and graduate into the impure lime-
‘stone with which the Calciferous group may be assumed to begin.
_ We thus have in the Primordial formation, in the belt now being described, at
ae three horizons of iron ore. The lower strata contain specular iron ore usually
of low grade, the middle portions, extending as far as the Potsdam quartzite, con-
te baining limonites, either impregnating definite strata, or filling what were once fis-
crops. ‘Finally, in the Ferriferous shales, we have interrupted deposits of limonite,
ii ni nelosed i in clay and often mixed with manganese. (No. 12885, U.S. G.S. Library.)!

‘The Balcony Falls section has also been studied by J. L. and H. D.

‘Campbell the section is as follows:

Feet.

> Ganiddticinics SEE es aan Wea ated ae cab oowewdy wees ow Se we ope 50
NU Fa Ss he cv aa nad pnd casio Wass <unbuwdanve snene - 350 -

ae ihn ian! ae kta Sa aaiceeurewEha soaies claw scedcusews 600

: Z 4, Sandstones (thickness not given).

a, eta ethan aod eees uigs veweanls Jeu onde dgcehess 180

BS 6. Scolithus sandstone ........ EE ee RT ES of Wee tae 340

IN orn cai ce coos aac wivncnesabicc satcon hens ccose 600

Aleta ys ain o hana Jing fads cee nkpnwwmewklecae nt cdus 2, 120

_ A comparison of this with the sections measured by Prof. Fontaine,
Ee n 1879, shows essentially the same succession of strata, although dif-
f fering materially in the thickness of the various divisions based on the
‘character of the rocks. Subsequently, Prof. Campbell added to ‘the
pr existent information of the section at Balcony Falls, by showing

that the primal series is present upon the southeastern slope of the
B lue Ridge, a short distance north of the James river. This was fol-
wed by a paper on the Snowdon slate quarries, by himself and his
ia, in which it is said that the sandstones are penetrated with Sco-
lit bus and dip beneath the Snowdon roofing-slate quarries.” An ac-
co mpanying ideal section, crossing the Blue Ridge 3 miles north of
James River Gap, represents the Primal series at the summit dipping
to the westward and on the eastern slope dipping at a high angle to
the ‘eastward and resting unconformably upon the Archean gneiss. *
at 1 Op. cit., p. 43.

~2 The Snowdon slate quarries. The Virginias, vol. 5, 1884, pp, 162, 163.
_ §Op. cit., p. 170,

‘i same shales, occurring under conditions similar to the iron and formed in like -

ed and crushed bands. Hence all of these usually appear in massive or rocky out-

: ‘Campbell with a slightly varying result. As measured by Prof. J. L. -

Fae ea ie THE CAMBRIAN. | Bis oe me ra oa or
a>. Byor, es Tk Campbell ednotuiias: from the stracture, that this. orfien™
Te of the Blue Ridge has been formerly spanned by a grand arch or series
of arches of Cambrian strata, upturned, perhaps, at the time of their 4
upheaval. ! 72
In 1885 Mr. H. D. Campbell a Hiahib a more detailed séehton of the
Blue Ridge at Balcony Falls, to illustrate the view that the Blue Ridge.
_at this point is a portion of an antic linal fold, over which the Cambrian —
‘strata formerly extended from the west to the east, forming a synclinal |
basin on the western side of the Blue Ridge. He described the Cam-—
_ brian section at Balcony Falls as follows: |

Feet.

1. Conglomerate 222.632 Jes 2... aot craw ote eee aig eee a 120

9: Randstene S22. Se a eae eee .--. 360

z 3. Slander. cist Sie Wonk oat Senlsemeessanwes padee *ic.. SOO
: 4. Heed sandetone 6 fia RR RR Ieee
6, Glatet 52 to = Seb. See ae ee ee ec eee ae saa 700

6. Mandeteiess9>. 623 so 3. SaGbek noo ee Vee owes oe eee ee

Te States. < 2s. 5 sc2% Foor Peele Ryo ptae Se ee ens) warigS Rae eee 120

GS; Scolithus sandstone 2: 223.5 iiss foo SR as Shee ee 350

He further states that, away Broth the river some distance, there is
about 600 feet more of scintbsiteae and friable slate before reaching the —
limit of the Potsdam formation.” This gives a greater thickness to the

_... Cambrian section of Balcony Falls than ee measured by either Bre . -
J. L. Campbell or Prof. Fontaine. —_- q

E The next complete description of the Cambrian in the southwestern *
re portion of the State is that of Prof. J. J. Stevenson, in his account of.
~ a reconnaisance of Bland, Gyles, Wythe, and portions of Pulaski and
Montgomery Counties. On the map accompanying the paper, the geo.
graphic distribution of the Cambrian rocks is shown for Montgomery,
Pulaski, and Wythe Counties. He includes in the Cambrian the lower —
Knox shales and the Potsdam, stating that the former are probably
equivalent to the hydromica schists of Pennsylvania and the lower part

-- of the Calciferous of New York ; the latter is the Potsdam of N ew York, ae
ae vastly increased in thickness. * "The Knox shales are described as bein iy is
reddish, sometimes streaked with white color, usually more or less”
greasy, often talcose-looking on the slipped surfaces. -The shales 2 are
- hard enough to form bluffs. The thickness could not well be: ast er

- tained, but it can not be less than 600 feet. oa EB,

ene - The Potsdam forms the great mass of Lick Mountain, is the sandstotie of Dra pe

Mountain, and is found along the southern border of Wythe, Pulaski and Montgon
ery Counties. The upper beds are alternations of sandstones and shales.

7
ed

At
_

B.
' Geology of the Blue Ridge near Balcony Falls, ies ae ab a modified view. Am. Jour. Sci., 3d 8 ery
1884, vol. 28, p. 223. ee
sag ? The Potsdam group, east of the Blue Ridge, at Balcony Falls, Virginia. Am, Jour. Sei, ads ay
vol 29, 1885, p. 472.
“8A geological reconnaissance of Bland, Giles, Wythe, and portions of Pulaski and Monta
Counties of Virginia. Am. Phil. Soc. Proc., vol. 24, 1887, pp. 86, 87. : :

Y
"Ss
*

ig am 7 7 =
esas + \

. hit ks that the sandstone of Draper Mountain is not less than 2,000
feet in thickness. The only fossils observed were Scolithus linearis, on
- ae Mountain. ;

ta South, the lower portions of the limestones are of Cambrian age.

brian shales is one of the problems to be studied in Virginia.

—-

NORTH CAROLINA.

- he Cambrian rocks in North Carolina are the extension across the
E border from Tennessee of the Chilhowee series with, perhaps, some of
% he Knox shales. The best section is that along the line of the French
Broad from Paint Rock on the State line eastward up the river to the

_ shales, or Upper Cambrian. The relation of the other portions of the

<=

4 bare res i TENNESSEE.
= Doses conglomerate.—The descriptive details of the Cambrian rocks
“of Tennessee are almost entirely derived from the work of Prof. J. M.
: Safford as published in the “ Geology of Tennessee” in 1869. A large

"amount of additional data has been obtained by the geologists of the
U.S. Geological Survey. At my request Mr. Bailey Willis, chief of
, evialachion Division of Geology, prepared the following notes upon

he geologic position of Prof. Safford’s Ocoee formation :

4 ris 'spbalechion Paleozoic area is bordered on the eastern side by a belt of clastics
* of very great thickness, which forms conspicuous ridges between the Archean gran-
ites and the calcareous Paleozoic strata. The slates, sandstones, and conglomerates
5 of this belt, characterized by lithologic similarities among themselves and distin-
znished by Marked lithologic contrasts from other rocks, fall into a natural group.

a -Semimetamorphic, they occupy mineralogically a position between the crystallines
and the unaltered sediments. Resting in many localities directly on the Archean
_ and containing fragmental granitic minerals, their apparent stratigraphic position
is also intermediate between the Archean and the unaltered sediments. For these
i. Peeseons, and in the absence of fossils, they have been placed by all the older geolo-
gists at the base of the stratigraphic column. Structural facts sometimes fall in with
“this stratigraphic arrangement, and where they do not faults have been assumed to
account for the superposition of the supposed older on younger strata.

oom Tennessee the type localities of these clastics are Chilhowee Mountain and the
ae) Ocoee gorge, and quartzites of the Chilhowee type, but not in Chilhowee Mountain,
ha ave been correctly placed above slates of the Ocoee type by Safford. Your own dis-
_ covery of fossils in the upper shales of Chilhowee Mountain appears to determine the
ge of all these sediments as Lower Cambrian or pre-Cambrian. But there is an as-
2 u amption which must be sustained, or the conclusion fails in its broad application.

"That i is, that the natural grouping of these strata by physical characters into a single
= ‘les proves them to be of one period ; this may be the result of similar conditions
: hic ich existed at different periods, and the natural group may include strata of widely

~ . > ¢

IT were ae Se ae See FE sa Se Re ee a ng BM es
= i+ Ng Gan TR AS wrt” ae 3 "¢ i ‘ gi-s

Sie de See ae
oS Tay gee aie anon : SSeS hired,
a ‘SUMMARY—TENNESSEE. bier nS, 3 OO

: ‘The base of the series was not observed by Prof. Stevenson, but he

_ InDutchess County, New York, on the north, and in Tennessee on |

- Whether the same is true of the arenaceous limestones above the Cam-.

_ vicinity of Warm Springs. The Paint Rock sandstone apparently is
the representative of the Chilhowee sandstone, and the shales the Knox —

_ section on the French Broad to these formations is, as yet, undetermined, ;

~*

i

appear to have suffered changes of form, which were both mechanical and chemical —

+ ville was a period of great transgressions beyond the limits of any previous subsi- .

= i: of ve ¥ Seka | ;
| Fein Vek? 2
gn a aoe Sica THE, -CAMBRIAN. ett Dee iy FS ge i

separated horizons. The latter is the fact. The Gkithavbe ideation: in Chilhowee
Mountain has been proved by fossils to be Lower Cambrian, but it is a synclinal —
mass isolated by faults, and the definite determination does not apply beyond its
limits. It is not connected with the Ocoee area, and the Ocoee rocks in- the type —
locality are so separated from strata of known age, that nothing definite can now be
asserted as to their correlations. Starrs Mountain, a “ Chilhowee” outlier 24 miles

- southwest of Chilhowee Mountain, contains a fossiliferous limestone apparently con- —
formably underlying the quartzite; if further study confirms this apparent relation, | 4
the quartzite is near or above the top of the Lower Silurian. Meadow Creek Moun- 4
tain and the Big Butt range, extending from 25 to 70 miles east by north from Chil- —
howee Mountain and assigned by Safford to the Chilhowee and Ocoee formations, are
determined on stratigraphic and structural evidence to belong to the Nashville period. 3
the last of the Lower Silurian deposits. ‘‘ Ocoee” strata of Safford, occurring south- —
east of Chilhowee Mountain about Cades, Tuckaleechee, and Weirs Coves, are known ©
to belong to the Nashville on evidence of strict structural conformity to the Knox —
dolomite over three extensive quaquaversals and through transition beds from the —
dolomite to the slates, The Nashville ‘‘ Ocoee” strata in this locality and in the Big
Butt exceed 12,000 in thickness and form some of the highest ranges along the N orth —
Carolina boundary. 4
If, as these facts prove, the great natural group of clasties along the eastern Paleo- |
zoic border is the result of conditions repeated in different periods, we should seek —
an explanation for recurrence of like conditions, and this is found in the relative :
extent of subsidence in the Cambrian and Silurian times. -
The Cambrian sea transgressed over the granitic continent under iach ednditionadl
that the constituent minerals entered into shore deposits, without complete decom-— 4
position; these conditions probably existed in the deep disintegration of the granite, a
as suggested by Pumpelly. The subsidence ceased during Knox time and the depo- |
_ sition of the Knox was followed by uplift which exposed the dolomite to the waves —
of the Nashville sea. The evidence of this and of subsequent subsidence is found :
- in conglomerates of Knox dolomite at the base of and interstratified with the strata —
of the Nashville-Ocoee in many localities. The beds associated with these conglom-
erates are arenaceous shales and sandstones, but higher in the Nashville series con- | :
formably stratified with these, and extending to basal conglomerates resting on the —
Archean, are deposits containing granitic fragments like those of the Cambrian- —
Ocoee. The stratigraphic and geographic relations leave no doubt that the Nash-—

dence, and the deposits derived from the granites in the later time were identical _
with those earlier accumulated from the same source. . = a

The semi-metamorphic character of both Cambrian and Nash yiliec neon: strata — iF
demands explanation which may possibly be found in their original composition and 7
in their common relations to thrust and resistence during Appalachian formation. =
Both series of rocks are thin bedded piles, both rest against the unyielding Archean
masses. Whatever pressure they received they were forced to conform to and the: yo
and which were induced by dynamic conditions. =

- The generalizations herewith submitted are derived from the detailed’ work of c
Messrs. Arthur Keith and C. Willard Hayes as well as from iy own studies and the
conclusions as to the age of formations have been reached through mutual coopera- ‘

tion. ? = 4 oS
Chilhowee sands tone. —The lithologic character of the Chilhowee sand-
stone is given as follows by Prof. Safford: Gr P - F

_ It is a great group of heavy-bedded sandstones, often dark, but generally weathering —
toa grayish white, and containing great beds of whitish quartzose sandstone, or quark
ite. Interstratified with the heavy-bedded rocks are, at some points, sandy shalt
and thin flags, often containing scales of mica. Some of the sandstones are coarse
: : Wer, eee!

. eS ee " SUMMARY —TENNESSEE. Ean, ee” BOgee

‘

ax in ¢ d approach fine pngloneese, It may be mentioned, too, that not unfrequently
yo he strata have green grains (glauconite) disseminated through them.

The sandstones of this group very often show the worm-holes, and the sandy rods
le thei, belonging to Hall’s species Scolithus linearis. It is the exception not to
meet with them. In addition to these, the surfaces of the strata sometimes show im- ;
Risesions, of fucoids. No other fossils, that I know of, have been found in this horizon
oon 7

_ This formation is by no means as thick as the Ocoee series; yet it has volume
! Bensogh to form conspicuous mountain ridges. It is not easy to determine its thick-
aed its maximum is not less, however, than 2,000 feet, and it may be considerably
_ more.!

- This general Mesertiphion 1 is followed by the detailed description of a.
uniber of sections. The lithologic features of this formation are much
_ the same in all of its presentations, from Virginia to Georgia.” 5
Knox sandstone and shale.—In the table of geological formations the
"Kos group is next in order above the Chilhowee sandstone, and its
basal member is formed by the Knox sandstone.* The principal rocks
F bof the Knox sandstone are hard shales and thin sandstones, heavier —
sandstones being interstratified with these. The heavier sandstones —
are fine or coarse grained, sometimes quartzose. They occasionally ,
~ abound in green grains. In the section of Webb’s Ridge, near Knox-
_ ville, the hard, dark, gray sandstone referred to occurs six times in_
beds from three to ten feet thick, and weathers into a buff, softer ma-
% terial. In general, the included tesers vary much in appearance. As
- before stated, beds of dolomite are met with in the division.‘

_ The thickness of these rocks can not be much less than 800 or 1,000 feet. In Webb’s
"Ridge, where eed are in less force than at many other points, the thickness is 540 ©
- feet.

- The strata are often ripple-marked, and sometimes covered with fucoidal impres- |

~ sions and ridges. Aside from fucoids, I have not met with any fossils in these rocks.
oa 72 *

4 alt may be mentioned as a prominent feature of this division and of the Knox dnais
overlying it that they present shales and sandstones of many different colors. The
| - rocks are pale green, brown, and red, chestnut-colored, buff, gray, and other colors.
a Brownish red, greenish, and buff are, perhaps, the prevailing tints. The colors are

a ‘often bright, and notably agreeable.

In reading the description of the Knox sandstone by Prof. Safford, I
; have failed to find any general or detailed section or description that
connects the Chilhowee sandstone and the Knox sandstone. Appar-
ently there is not any section known in which the two are seen in strat-
- graphic relation to each other. From the character of the section
_ and the sedimentation, it may be that the Knox sandstone is the repre.
“ sentative of a portion of the Chilhowee series, the former being the
off shore deposit, while the Chilhowee sandstone accumulated near the
_ shore.

The Knox shale is largely a variegated shale, with interstratified
eds of thin layers of blue limestone, which is often oolitic.

-- 1Geology of Tennessee, pp. 198, 199. 3 Op cit., p. 158.
2 Op. cit., 1869, p. 203, 4Op. cit., p. 209,

7 _

Ses weg oe 4 tig Seis ie 5 So EN ey Sa NR Se OT tea > |
. Ad pe sa > ’ iad > a" 7 “ - , vs

- of demarcation must be drawn near the Wee of the dolomite.

ta ‘ Pgh <7 zB Ser ; ~ <4. —e ‘ 3 55 hy ia i . : = S
De ae ae Pe THE “CAMDRIAN.- =e Ga ei picid

J
ae

The Seianicaig wands § in the sda reall ‘of the division are pea oitiaepnbas £ toward i
the top, they-generally become more abundant, increasing as we ascend, until finally.
the shales disappear, and the blue ooliticlime stone, and dolomites are the on. 7
rocks. In this way the shale division runs into the uppermost one," qq
In the northeastern part of the State the shales, as a division, are not well chavastl
terized. As already stated they are much mixed with beds of limestone and dolo-—
mites, and lose, in good part, their distinctive features. Moreover, in this region
there is little oolite rock. A portion of the shale appears to be replaced by a blue
limestone containing thin clayey seams, which give the surface, especially when
weathered, a striped appearance. This striped rock occurs, too, further south, se
place being at the top of the shale.
The thickness of the Knox shale is not easily determined.. What is said in roferal
ence to the thickness of the strata in Poor Valley * * * applies ini : ie
may place it as an approximation at 1,500 or 2,000 feet.!

Prof. Safford states that fossils occur in a blue limestone interealated
with shales, sometimes quite abundantly, both in the compact and oolitie
layers. Toward the top of the division and in the blue rocks of the
succeeding division they are seen at many points. The shales them.
selves are occasionally fossiliferous. It was his intention to describe
the species in the appendix of the volume, but we find oely:; a list of
names, as follows: ey : ,

.

Crepicephalus similis, Safford. ee 4
roanensis, Safford. .
tennesseensis, Safford.

Lonchocephalus fecundus, Safford.

Agnostus arcanus, Safford.

Lingula prima? , Conrad. Ea,

A large collection has been made within the last few years ee the.
localities from which he obtained his specimens, and from many others ~
in Tennessee, that indicate this fauna to be a portion of the Upper
Cambrian or Potsdam fauna. The same fauna extends up into the base
of the limestone for a short distance. The entire dolomitic series is”
referred to the Knox group by Prof. Safford, but I think that the Tine”

‘As a whole, the Cambrian group in Tennessee is represented by a
great. series of sandstones at the base, succeeded by a series of shales
that become more and more calcareous toward the top, where they pass
into the dolomitic series, forming the base of the Silurian (Ordovician)
-- system. During the progress of the resurvey of eastern Tennessee by

the geologists of the U.S. Geological Survey Dr. Cooper Curtice found
a few fossils in the shales interbedded in the quartzite of Chilhowee
Mountain, and in 1889 I found a few specimens in the shale about 20
feet above the quartzite in the upper shale bed. The study of the fos-
sils collected by Dr. Curtice and myself proves that the Olenellus or
Lower Cambrian fauna occurs in the shales of the quartzite series of
-Chilhowee Mountain. This fauna, with that found in the upper portion
of the Knox shales and the base of the dolomite, gives two distinct

1 Op. cit., p. 211. 2 Op. cit., p. 212,

nae a fe = a

Al es oe RE Se Oe

e > > -

ee Shericbusin the Soniteaw of. Tennessee—the Sawer Cambrian and the
_ Upper Cambrian. Between the two there is an unknown thickness of
shale, i in which fossils have been found sparingly, but not in sufficient
numbers to determine the presence of the Middle Cambrian fauna. If
_ the definition that the base of the Cambrian is to be drawn at the lowest
. _ horizon i in which the Olenellus fauna is found is applied in Tennessee,

4 x. the Chilhowee sandstone will be referred to the Cambrian. ;

_

7 ; GEORGIA.

The published information relative to the Cambrian rocks of Georgia
Ss _ 1s. largely contained in the work of Mr. George Little. It is summed up

in the compilation prepared for the Department of Agriculture, under .

~ the direction of Mr. Henderson, as follows :

_ Acadian.—Along the western escarpment of the Cohuttas exist beds of semimeta-
Fisorphic slates, and conglomerates, apparently of very great thickness. To this form-

3 ation, in Tennessee, has been given the name of Ocoee group, from the Ocoee River,
along which, near the line of Tennessee and Georgia, the rocks appear to have their

.. _ greatest development, or at least are most prominently displayed.

_ The group as yet is not known to contain fossils, but has been referred on the ground
ay of its supposed stratigraphic relations to the Acadianepoch. A sandstone of several
4 hundred feet in thickness is conspicuously displayed in-steep ridges or mountains
_ skirting the western base of the Cohutta, Pine Log and Allatoona Mountains. This

-
u
oy

is the Chilhowee sandstone of Tennessee, and is believed to be the equivalent of the |

> Potsdam sandstones. In Tennessee, Scolithus impressions—worm holes filled with
sandy rods, somewhat softer than the body of the rock—are mentioned as a common
; __ characteristic of the sandstone by Prof. Safford, and indicate a probable identity in

_ age with the Potsdam sandstone of New York. These markings have not yet, so far

- as known, been observed in this State, but the sandstones are often filled with small

‘rounded concretions, that disappear from the weathered surface, and give much the
a appearance presented by a cross-sectiou of the Scolithus rods in sandstone.

_ This is succeeded by hard glauconitic shales and glauconitic sandstones, associated _

with siliceous limestones, found in a broad belt of country along the Coosa River,
= and give rise here to what is known as the Flatwoods. Some portion of the same
group is found in a belt of country in the eastern portions of Gordon and Bartow and
the southern part of Murray, and also come to the surface again for a few miles in
_ sterile ridges on the western side of Whitfield County, between Dick’s Ridge and
x ~e ee Chatioogais Mountain. Trilobites are found in some of the shales and limestones,
_ and are abundant in the Flatwoods, near Livingston, in Floyd County, _ 7
_._. Aprominent mineral characteristic is the common appearance of green sand or
glauconite in the shales and sandstones, and sometimes in the limestones. ‘This green
__sandjmay be found, on close examination, in most of the shales and sandstones,
_ and is sufficiently abundant in some to give them a decided green color. * * *
ca Knox shale-—Shales and limestone of an estimated thickness of 3,500 feet. The
Z. shales are more or less calcareous, and are generally of a light green shade of color,
below the water surface, but weather into a great variety of shades from buff to red,
= + blue, green, brown and black, but is most generally some shade of brown. These
_ shales exist in all the counties in northwest Georgia except Dade, and are found in a
_ number of long valleys, varying from halfa mile to 1 or 2 miles in width, constituting
4 ane large part of the area of cultivated lands in this section of the State. Among

ea . ‘Valleys of Whitfield, and the Chattooga Valley of Walker and Chattooga.!

- ? oo
A _ 1 Henderson, J. T.: Geology (of Georgia). The Commonwealth of Georgia; the country, the people,

7 ead pentnesins. Alois, 1885, pp. 83, 84. =

#8 igi ie _ SUMMARY—GEORGIA. See 303

_ these are the Oothkalooga Valley of Bartow and Gordon, the Cooehulle and Dogwood.

poe er ed ab — oS os ee Ue OP ee ee, ed? oe
Kae eR ies ee ee, aa ee Tee rer ey hs ge
ah See , i ae

*.
, ~o

.

thickness of the formations referred to the Primordial is 8,000 feet, and —
to the Knox shale series 2,400 feet, making a total thickness of 10 400

~ such estimates must be carefully revised, as the LEST: of the Knox | 4

top downward :

Cambrian.

- 8
- ;
)
‘ \ -°
eee

ite that he considers to correspond to the Rome sandstone. It has a

r Ae ek ae oe an oe Rg. ke Seite re es Rear a oe an
: 3. > a Pod V . w= ,, ay la ;
Sy aie ey Mace eeeee me oe Bh ge See uN
fail : oy ack i leh x aie ee 3
ig + THE ‘CAMBRIAN. “Ue 4 Ren SO eas igen
*

eed ©
“>

As noticed in the historical reviews Mr. MoCutchen’s éstimates of thea

feet. The estimates of fhe author we have just quoted assign to the |
Knox shale a thickness of 3,500 feet, which will give a still greater _
thickness for the total Cambrian section. I think, however, that all

shale series are very much disturbed by plications and faulting..
_ An unpublished section, by C. Willard Hayes, of the Appalachian Di |
vision of the U.S. Gedlosieal Survey, extending from Rome, Georgia, |
to Gadsden, Alabama, gives the o ae Series, extending from the

}

Silurian. | Knox dolomite. ......-.-... Nee a Pony ape eS soot 4, 000-5, ,000.

( Thin bedded seamy limestone, sometimes blue and mass- | 4
ive.

Yellow shales, calcareous, grading into seamy limestone.

Earthy limestone interbedded with shales, often want-
ing; locally carries nodules of chert.

_Yellow shales. ‘

Oolitic limestone; thin beds in light green or yellow
shales. ;

Variegated sandy shales, purple, green, brown, etc .... 1, 600-2, bi

a
ee
> —_

Connasauga shale,
A\natmnnnlt

—— -~

Thin beds of highly colored sandstone; red, purple, and a
green; show ripple marks and sun ‘cracks. Beds 1 a4
to 12 inches thick with interbedded shales. Maxi- =
mum thickness shown between Rome, Georgia, and | er
Big Cedar Creek 3. jo c- in ssh es can sp oe cone odes 1, 300-1, 800

ome

a 3

stone and
Weisner
Quartzite.

Green shales, with thin, hard, siliceous beds, 4 to 2
inches thick, or layers of flat nodules. Maximum | ee
thickness at Georgia-Alabama line .............----. 700-1, 500

Rome Sand-

Fine yellow or brown shales, containing some beds of . <a
blue Limestone ..2 2 oc tagh ak to ces us 3 once bees y 1,0004
Heavy beds blue, seamy limestone ....-....-..-.1.---. . 0025s
Yellow or green clay shales, with thin beds of blue : Te
limestone contorted and filled with calcite veins.
Sometimes the shales contain siliceous nodules. Al-
ways highly contorted. Cover a large area between | —_~
Rome and Gadsden, and form the “ Flatwoods” of
Coosa Valley. Thickness not known; probably not
2 , Joss LHAM 25. tcc ebee So cnatrat ene that daneneceeeane 3, 500°

~~

Coosa shales.

In a recent paper on the valley rocks of northwestern Georgia, Mr :
_ Hayes assigns a thickness of 1,600 to 2,000 feet to the Connasaugs ra
(=Montevallo of Smith) shales; 2,000 to 3,500 feet to the Rome sand
stone and Weisner quartzite, and 3,000 feet plus to the Coosa shales.! if a
In a section at Mount Weisner, Alabama, Mr. Hayes found a quartz: ut

thickness of about 800 feet, and is in the form of lenticular masses of
white quartzite; sandstone and conglomerate occur at the base an a

1The Overthrust foults of the southern Appalaphians. Bull. Geol. Soc, ISS vol, 2, Feb, 180,
p. 143, pl. Se t 3 Pi : “*S

. oll : oe ‘pets art -1$ ae A, ~ - payee ore en UL i Se a pense

ones ra

a?

See « a Ths S,

ace a portion of the Rome sandstone. In Indian Mountain it is
m uch thicker than in Mount Weisner, and consists of several beds of
‘quartzite, with intervening masses of yellow sandy shales.

The fossils collected from the Coosa shales by Dr. Cooper Curtice
‘ Indicate as studied by me, thé Middle Cambrian fauna of the northern
\ ppalachian section. The Connasauga shale is correlated by its strati-
Z Seances section. In Mr. Hayes’ table the Rome sandstone and Weisner
5 quartzite are placed on the same horizon with the Knox sandstone,
x Potsdam or Chilhowee of Smith and Safford. That the correlation by
” Messrs. Smith and Safford of the Weisner quartzite with’the Chilhowee
$ is probably incorrect is supported by the fact that the fauna of the
Joosa shales belongs above the Chilhowee sandstone in sections where —
$ Fite: succession is undisturbed. The Chilhowee sandstone fauna is the
type of the Lower Cambrian, and the Coosa shale fauna is that of the
_ Middle Cambrian.

~ When the maps of the Po iaors region of ebraia and Alabama are
Epablistied geologists will have the data for the geographic distribution
> of the Cambrian rocks, and also sections showing the relative position,
thickness, and the variations in the character of sedimentation from
the south to the north as the formations pass to the north into Ten-
_hessee. " |

te _ ALABAMA,

d Es Our knowledge of the Cambrian rocks of Alabama is largely obtained
_ from the Report of Progress for 1875. The nomenclature adopted for
the fossiliferous sedimentary rocks up to the base of the Knox dolomite,
by Prof. Safford, in Tennessee, is followed by Prof. B. A. ‘Smith in this
‘report. To the Primordial or Cambrian series he assigns the Acadian.
epoch, or the conglomerates and slates corresponding to the typical
_ Ocoee section in Tennessee. To the Potsdam epoch he confines the
i Chilhowee sandstone of the Tennessee section. The Knox sandstone
and Knox shales are referred to the Canadian period. The term “Cal--
Se rus sandstone” is used as the equivalent of Knox sandstone, and
“& Quebec shales” of the Knox sbales. The section of the Acadian slates
and conglomerates in Talladega County is considered by Prof. Smith
typical of this series in Alabama.'. The description is as follows :

: < The western border of the Metamorphic rocks in Alabama is formed by a belt of
slates and conglomerates, semi-metamorphic in aspect, and of varying width, but per-
haps ‘of an average width of six miles. These rocks, which in every respect seem to
Piss 2 the exact equivalents of Prof. Safford’s Ocoee Slates and Conglomerates, are re-
- fe rred like them to the Acadian epoch.?

: ‘The stratigraphic succession of the beds is not well determined.
q 7 here is a belt of greenish talcoid, or hydro-mica slate, and a series of
conglomerates which are Spinioiiiias a slaty, arenaceous rock, but often

OR eport of Progress of the Geological Survey of Alabama for 1875. Montgomery, 1876, De. 13517.
Tag Op. cit., p. 127.
A ; ‘Bull. Pe sa0s, SS

‘4 “- —
sah ? PEE » ake i ae Tay. Sat J ve
. y on ™ Z A

rs ge “5 | SUMMARY—ALABAMA. eRe cote kc SO ede

raphic position with the Knox or Upper Cambrian shales of the Ten-—

_

'
=

*

_ metamorphosed Potsdam sandstone. In the disturbed region | of the Kahatchee Hills, —

burrows of a marine worm, Scolithus linearis. Upon the bedding planes of the sand-

and these with dolomite, so that three groups are usually closely associated geograp!

division, The bedding planes of the sandstone commonly show ripple marks al

quite massive, and made up of lanips of pebbles of re quartz
~ and opaque white feldspar, held in a matrix of greenish talons matter.

Of the second division, or the Potsdam, itissaid: 2 ae

Next in ascending order, to the slates and conglomerates of the preceding group, | |
comes a series of sandstones which form the most conspicuous mountains outside the
Metamorphic and Acadian areas. The direct superposition of this sandstone upon —
the slates of the Acadian age, I have not seen in Alabama, unless on the eastern edge
of that belt, the prominent sandstone or quartzite ridge be, as seems quite probable,

also, half metamorphosed slates are seen, some of which may belong to the Acadian
epoch, whilst others are evidently altered Knox shales. : =

Fine-grained conglomerates, heavy-bedded sandstones, and sandy shaleé make up .
the great mass of the rocks of this formation. I have noticed, also, occasionally,
masses of a brownish porous chert, which, from its association with the ee
seems to be of the same age. :

In general, the rocks of this formation are hones bedded, almost massive, and the
higher crests of the Potsdam Mountains are usually covered with huge blocks of
sandstone and fine-grained conglomerate. In the lower parts of these ranges, sand y
shales are the prevailing rocks. * * * The most characteristic markings of the =F:
rocks of this formation are the sandy rods, caused by the filling in with sand of the |

stones, small rounded depressions or dots mark the cross-sections of these Scolithus ;
burrows. As yet I have found no other marks of organic origin in strata of thi is.
Hosmzon. =" .*.* “3 “f

The nature of the rocks of this group, conglomerates, sandstones, and sandy shales,
the fossil markings, principally the burrows of marine worms, etc., all point to as

shore origin. a
From the preceding descriptions, the equivalency of the Chilhowee a

sandstone and quartzite with that of Alabama is extremely probable,

if not certain. | a
Of the succeeding formation, the ies sandstone the hee di

- seription is given: ;

The rocks of this group succeed next, in ascending order, the Potsdam sandsto
and they are often, no doubl, found resting directly upon that rock. I haven ;
however, often seen them in this position; but much oftener just on the southeast si de
of a fault by which they have been raised to the level of a much higher formation. .
This sandstone is more generally associated with the shales of the next higher group, »

on:
rage
p

ically as well as lithologically. a
A calcareous sandstone, sometimes thick, sometimes thin bedded, is the charact er:

istic Knox sandstone.
It is associated with hard calcareous shales much like the aiites of the next high

irregular raised markings, which are commonly supposed to be fucoidal impressia 6.
The bedding planes are also frequently smooth and shining as if polished. Ge :
grains of glauconitic mineral are usually to be seén upon a fresh fracture of thes
stone; upon weathered surfaces the brown color of hydrated ferric oxide is
the. maak éf the decomposition of this mineral. The colors of the Knox sands
are pleasing to the eye, and are gray, greenish brown, buff, chestnut colored,
Beds of dolomite, impure and cherty, are found in the upper part of this formatic i
two such calcareous beds were noticed in the exposure of Knox sandstone a ms

Jackson shoals and also at Helena. * *° *

rs

- *.

_

1 Op. cit., p. 13-15.

stdin of thie’ mountains enumerated in a previous section ; but it is not always
sy to ‘digtinguish it ; since, however, these ridges of Potsdam snidstine have a well
_ defined belt of Knox iitalos on their eastern and southeastern flanks, the Knox sand-
_ stone, probably i in most cases, intervenes between the two.!

It will be noticed in the description given of the Knox sandstone
. “that its direct superposition upon the massive ‘“ Potsdam” sandstone
Se not been observed. I think that as in Tennessee the Knox sand-
_ stone may be, in part, the equivalent of the sandstone referred to the
Potsdam or the Chilhowee sandstone. It is probably the accumula-
ica of sand and shale deposited while the sediments of the more
_ massive sandstones were accumulating nearer the coast line. :
_ The Knox shales rest conformably upon the Knox sandstone series
and correspond in their description closely with the Knox shales of
& Tennessee. Of these beds Prof. Smith says:

oo The characteristic rocks of this subdivision of the Knox group are calcareous shales
| 3 of bright and agreeable colors, usually gray, buff, greenish, brown, chestnut colored,
__andred. The shales are tolerably soft, and in some portions in weathering, break up
into small angular pieces resembling shoe pegs. Strata of dark blue limestone, some-
times banded with aggillaceous layers, are found, especially in the upper part of this
_ division. The weathering of such limestones brings into relief the bands or stripes
of argillaceous matter, and the limestone appears very distinctly banded. Where
_ these impurities are ae so regularly disposed in layers, but in patches, the promi-
nence given to them by the weathering away of the limestone gives them a striking
eecomblance to half-exposed fossils.
In some places layers of dark colored oolitic limestone have been observed, one of
- the best localities of this peculiar rock being at the foot of the mountain at Alpine
eention 3 in Talladega County.

In the upper part of the division blue limestone layers become more frequent, and
£ ithe transition into the overlying Dolomite is so gradual] that a line between them
peetolonieatiy 1 is hard to draw.?

au

_ The only instance mentioned to indicate the relations of the so-called

P Potsdam sandstone to the Knox shales is in the following paragraph:
= Between the Ladiga Mountain and the hills of Acadian slate in Calhoun County,

_ there are numerous small ridges of Potsdam sandstone, on the flanks of which the
3 ‘Knox shales seem never to be wanting.®
. ~ No fossiliferous strata were observed in this Peer
, The distribution of the Cambrian rocks of Alabama is shown ona
a “map accompanying Prof. E. A. Smith’s outline of the geology, published
in 1878. On this map the geographic distribution of both the Cambrian
ag Lower Ordovician rocks is delineated under one color called the
Silurian. It includes all the formations from the Clinton down to the
F Acadian. Of these formations the Cambrian includes, at the summit,
_ the Quebec or Knox shale and Knox dolomite, or at least the lower
portion of it, and subjacent to this the Calciferous or Knox sandstone,
_Veneath which the Potsdam and Acadian are placed, the latter forming
he base of the Paleozoic series.‘

= “Top. cit., pp. 17, 18. : ~ 2Op. cit. ,p. 19. 3Op. ‘cit, p. 20.
~ Outline of atte geology of Alabama. . Berney’ s Handbook of Alabama, 1878, p. 139.

ne

> al A ae © ee Are ©. Jo tee ta ‘a obi ae - 2
BT eer pS eee Ae ee ee ee Ree, ees aes beh Ss Says Shota i ee eae
wR7S ms (. aie > ¢ ~~. gress ; r uae ‘|
j = Pa * “ % F v ee . ow

‘

- Cambrian rocks extend 400 miles farther to the northeast from Quel ic"
to the northern portion of the peninsula of Gaspé; but there is now ¢

gos. St PR ASS “THE CAMBRIAN. roe tis NES rota aL,

- Cambrian recognized are, in ascending order, as follows: ‘The ‘Coosa
__. Shales, the Choccolocco or Montevallo shales, and, inferbedoms with
seams at the base, and pass above “into the Montevallo shales,
variety of colors, such as olive, green, brown, chocolate, yellowish,

ana gray dolomite occur which are difficult to distinguish from similar

‘with the Chilhowee formation of Prof. Safford in Tennessee.?

brian in Alabama it appears that they are the continuation of those re- ;
ferred to the same group in Georgia and Tennessee, though varyidieg

- Tennessee, and ‘aio Georgia and Alabama, the rocks of this pre- “Ona i

and the long, narrow Archean axis of the Gaspé peninsula. The ex-
posures of the Cambrian on the coast of Labrador, opposite the Straits

: ; a
é aa of <- * . a.
ee ; cnet - - 36" ee oe ¢ Ae | F
- = P “/ ? 4 he. os 7 »
') . ~ . »? r Ge

“In: a report. on the eres of the Uahaba Coal Field 1 Prof. Wigene Ast
Smith describes the Cambrian rocks as they occur in the Coosa Valley 5
of northeastern Alabama. The maximum thickness given is 10,000
feet in the eastern part of the Coosa Valley. The subdivisions of” the |

the last named, the Weisner quartzite. ”!
The Coosa shat are described as thin-bedded limestones with clay

which form a considerable thickness of sandy shales of a great.
etc. In the upper part of the Montevallo shales beds of blue limestone

rocks occurring in the superjacent dolomite series. Lenticular masses
of quartzite many hundreds of feet in thickness occur in the Montevallia
shales. This quartzite is named the Weisner quartzite from its typical
locality at Weisner Mountain, east of Jacksonville, and is correlated

From our present knowledge of the formations referred to the Cam. ;

somewhat in the local eget of sedimentation, thickness of beds, and
lithologic characters. > ® d

The section of Mr. C. Willard Hayes, described under Ceoneiet em-
braces much of the Cambrian strata that passes into Alabama, and
should be referred to in this connection. ine, Dp. 304.) a

. es a . Say
- 2

For a distance of over 1,200 miles the pre-Cambrian lands formed the
eastern boundary of this province during the deposition of the sediments:
of Cambrian time. From below Montreal to the foot of Lake Champlain _
and thence southward to the crossing of the Hudson, below Pough- x
keepsie, New York, and on across New Jersey, Pennsylvania, Virginia,

brian land form an almost continuous outcrop at the present day. The
interval of over 200 miles between the Archean ridges of eastern Quebeo oC

of Belle Isle, and those of the west shore of Newfoundland, have been
included in the Atlantic Coast Province, but they are quite as much a
ma

fr Geological structure and description of the valley region adjacent to the Cababa Coal Field. Geol

Survey of Alabama. Report on the Cahaba Coal Field, pt. 11, 1890, p. 148, (issued J paeet 1801). a
2Op. cit., pp. 148, 149. on

. dL FAdee be, ae Tbard,.* .. “a a " re * TY
‘ vei Page CAs | Sasi bad a m4
eas FH te at. a Poi i:
x 2 ‘- uf

~*~

Lg aa ;
Be es wie 4
Sn p part of the ‘Appalachian Proves by fauna and pi iiont ehataciae and
are considered as a connecting link between the two provinces. The
% Eisbrador deposits are on the north shore of the Cambrian sea, but
ES those of the west shore of Newfoundland are, in physical character and
organic remains, the practical continuation of the sediments of the east-
_efn side of the Appalachian Province. If this correlation be made, the
_ pre-Cambrian shore line is carried 400 miles farther to the northeast
: Bad thence to the Straits of Belle Isle, giving a nearly direct line
of over 2, 000 miles that may be included in the Appalachian Province
_ with its Ohnadian extension. Along such a great extent of coast line
¥ ~ oneexpects to find evidences of varying sedimentation, both in character
and amount; and an examination of the.various geological sections of
eNewfoundland, the river St. Lawrence, Vermont, New York, and south
along the Appalachian range to Alabama, shows the most marked vari-

* ation, both on the strike of the strata and in proceeding westward
prom the ancient shore line.

tess impure limestone. On the western shore of Newfoundland, over

~ bly upon 600 feet or more of slates. For 375 miles along the south shore
| _of the St. Lawrence, from Cape Rosier of Gaspé to the vicinity of Que-

_ bee, the strata referred to the Cambrian consist, according to Mr. James | :
~ Richardson, of quartzite, with intercalated beds of conglomerate holding — -

7 limestone pebbles, the whole forming a series 600 feet in thickness.
_ This is superjacent to 700 feet of gray sandstone, also carrying con-
- glomerate, while beneath this a limestone, with conglomerates and
_ bedded sandstones towards the lower portion of the section, extends
_ downsome 700 feet more, giving over 2,000 feet as the entire thickness of
4 the section. Owing to the absence of paleontologic data there is some
Bs | ‘uncertainty i in referring all of this series to the Cambrian. In some of
. the pebbles in the conglomerates of the upper portion a number of
4 species of the Olenellus fauna were found; but no one of the three great
- divisions of the Cambrian has been aiatinaiy recognized.

_ In the vicinity of Quebec the stratigraphic succession from below up-
ward consists of a succession. of black, green, and gray shales, with hard
and heavy bands of green, sometimes yellowish white, quartzose sand-
- stones, This is succeeded by greenish, grayish, and blackish, with
_ occasionally dark reddish or purplish tinted shales, with a band of hard
F " grayish sandstone. Above the latter bright red shales, with thin green-
~ ish or grayish bands, which in places are often calcareous, extend up
_ through red, greenish gray, and black shales withinterstratified masses,
_ often lenticular, of greenish and grayish Sillery sandstone. In the up-
per part of this last series Obolella pretiosa occurs. <A thickness of
from 5,000 to 6,000 feet is estimated for the Cambrian series, beneath
the graptolitic shales of Point Levis..

-

-

=

Ca . : dy
9 TSSOP" ae. ¥

" SUMMARY—APPALACHIAN PROVINCE. es 809 BS,

On the Labrador coast the rocks are sandstones followed by more or

ed, 000 feet of alterifatin g limestones, shales, and quartzites rest dontasiies

a lt she be noted of this section that the limestones of western New- .

Bae 310 pos ena ae > eRe CAMBRIAN. = peel Se usa

stone occurs in the argillaceous shales, in which a fauna of Upper os

: ~ point this shore deposit is traced without interruption to the Massa
_chusetts boundary; and then, with more or less interruption, to the

h

- thence, with some interruption, into Georgia andAlabama. On all this 4

grained sandstones, shales, slates, and limestones. In southern Ver-

~ are absent, and that the section is composed almost entirely of arena-— j
-ates of the Point Levis, graptolitic,Lower Silurian (Ordovician) shales. _

_gimilar to that now found in Labrador and Newfoundland.

ton Mountain anticlinal or the belt extending southwesterly from Gand 5

-ceous Shales. More or less arenaceous matter is associated with the —

Pp os ~. q
* <s .<
hieee eg ee
Fe ah wy.
z Pepa - Ve pine

foundland ee ike lower portion of the saath shore of the St. ‘Lawrence 4

ceous and argillaceous sediments. A limestone conglomer ate, near the
upper portion of the Sillery, contains bo wlders carrying the Olenellus— 3
fauna, and the Upper Cambrian fauna bdccurs in the basal conglomer- .

These bowlders appear to have been derived from a limestone series” 4
The strata referred to the Cambrian, on the western side of the Sut.

bee to the Vermont boundary, consist of more or less of the Sillery |
series, as found in the vicinity of Quebec; and, according to Drs. |
Selwyn and Ells, of a subjacent series of hard quartzite rocks interstrat.
ified with mica schist and black slate. The volcanic series, referred to 4
the Cambrian in this region, indicates that during earlier Cambrian |
time the volcanic products were deposited contemporaneously with the —
included sandstones and slates, thus giving a phase of sedimentation —
not known elsewhere in the Cambrian of the Appalachian province. - ;
For this reason and from the fact that there is not any paleontologic —
evidence of the age of this volcanic series I am inclined to think that
it may belong to some pre-Cambrian terrane. F

Entering the northern end of the valley, between the Green Mound
tains and the Adirondacks, a sudden change occurs in the sedimenta- _
tion. At the base, the Olenellus fauna ranges through 1,000 feet of —
magnesian limestone, and for 250 feet higher up in arenaceo-argilla-—

limestones, and, about 2,000 feet above, a gréat lenticular mass of lime- —

brian aspect is found. At other localities this fauna occurs in the
shales themselves and in a brecciated limestone at the same relative
horizon. As far as known the upper portion of the Cambrian is
formed of the shales. Proceeding southward and nearer the old coast |
line in Addison County, Vermont, the limestone series is found to.
graduate into the Granular Quartzite or the beach sand. From this

Hudson River below Poughkeepsie, New York. It is taken up again-
in New Jersey, and thence may be followed, with some interruption,
across Pennsylvania to Maryland, whence it extends as an almos t
continuous formation across Virginia into Eastern Tennessee, and 14

long line it forms the basal member of the Cambrian; and wherever fos- S: :

_ sils have been found in it they belong to the Olenellus or Lower Cam Me

brian fauna. a
The offshore, or deeper water deposits, are ropieoeae by finer-

‘ ; a Ney «
t : ' Pie oh, 4 aye
~ g te - 4 — vinnie

. ee . ‘TI puv 1 sdem uo sloquinu — } we Ree
SuOTIONS OY} YIBONEG JoquanU oYL “YOUT oy} 02 Joey OOF'9 ‘1UOS THOTMP.A ‘POULAIA UEIYoreddy O43 Jo SUOHOaS—"Z ou |

d

s

§eL109

aT]¥00] om 0} puo

mre ae a AMMARY Se et
they form the rooting slate belt that hee ufo New York, where
ion: eat some 12,000 feet of shales, eres and inter-

-

HAT

2
ZLabrator —

° Hs ei. eee ae $5
= -EE nn i Northern Fermont,
e\s
; + lo oO
a
|

«
‘c

é

———

ll iter C0.N. 9

J

e: county, the pascal seadtéate rests upon ‘the pre-Cambrian and contains —

CS tk

rt

os

Sg SoS R I Ae slates CASE noi Ve ae eae har,
x.

A i- s . a wes ¥s ee fe ee , oe ‘ $a." ae 4 rs, % . "e ¥
. oe ) ee Pas A bes “NE = Se aS " “= Yeap as 7 +
ray A er x , » 4 ar) me Mae iso h can tS: . at a

that the lower portion of the limestone is of Cambrian age, the same |

_-are characterized in their upper portion by the Upper Cambrian fauna,
which passes above into the base of the great limestone series. As far ©

Jersey, and into New York, the argillaceous material accumulated in —
_ relatively small proportion to the arenaceous beneath and the calcare-

ment. To the north these conditions remain until, in northern. Ver- |

’ ee RS hope ae
312. bie es te 5 3 “DHE ‘CAMBRIAN.- eg eB Le Ta

‘the Olenellus fauna. A few remains of the latter have also been found i in
the immediate superjacent limestone. The Middle Cambrian and Upper
Oambrian faunas occur in bedded limestones As the quartzite exposed —
on the eastern side of the limestones of the ‘Marble Belt” represents —
but a very small portion of the great series of shales, slates, ete., of
the Cambrian on the western side of the “ Marble Belt,” it is Frobebiell

as in Dutchess County. This observation also applies to the basal —
limestone in New Jersey and Pennsylvania, where there is very little - Ԥ
thickness of shales between the basal quartzites and the limestone.!

In central Virginia the lower 1,000 feet of the section is composed of —
an alternation of shales and sandstones, while the upper 1,400 feet is .
nearly all shales and slates, capped at the top by a Pore siliceous —
limestone. %

In Tennessee the quartzite is developed to a great thickness. The
quartzite is of Lower Cambrian age, and the Knox series of shales —

as known, the conditions in the sedimentation of the Alabama and
_ Georgia sections are very much like those of Tennessee. — eee.

‘Briefly summarized, the sediments along the southern portion of the
coast line are anintaties followed by shales and limestones. More or
_ less-variation occurs, but, as a whole, thechange is gradual as we follow —
tlie coast line to the north. In central Virginia, 300 miles to the northeal
east, the argillaceous deposits are more abundant in the lower portion, — a
and they form the greater part of the upper series ie the base of the a
‘limestone. ;

From Virginia northward across Maryland, Ponngpieuatl and New 4

ous above. How much of the latter is to be referred to the Cambrian,
is yet undetermined. Our knowledge of the series in Pennsylvania —
and New Jersey is too limited to make an accurate compete with —
other sections.

In western Massachusetts and Vermont and eastern New York there
are immediate coast-line deposits and also those of deeper water. —
_ Along the coast line there was a great accumulation of sand, followed —
by some argillaceous and then calcareous mud. Farther to the west
the argillaceous material predominates and the arenaceous. and cal- es.
eareous forms but a slight proportion of the great thickness of sedi-

mont, the calcareous matter predominates in the lower. portion of the 4

-17The announcement was made at the December meeting of the Geological Society of America at —
Washington that the Olenellus fauna had been found in the quartzite in New J: ersey, and na
fossils in the limestones above the quartzite in New Jersey and at Rutland, Vermont,

L- a ee AS Pee <4 ee eM ee ee ee ee er Sf ee TF oes Ue
yes prota yes Mey Aes Te Re PN Seer ie ete te eee oe eee ee ee
ots “i; wa te y : 7 “ta ‘ e
. CA AY 4S 3 rt vig .

2 ey Ie
Ves | ny,
~~

“sUMMARY—UTAH AND ‘NEVADA. : 313

, “section, and the upper portion is ‘nos entirely argillaceous. In the
4 vicinity of Quebec, sandstones and shales make up the section, and
along the Lower St. Lawrence, shales, sandstones, and limestones.

_ As a whole, the Appalachian Province is one of varied sedimentation,
and, from the character of the sediments and determined fossils now
_ fonnd in them, they were largely accumulated along a gradually sinking
coast line. The northern and western shore line exhibits only the con-
tact of the sandstones of the Upper Cambrian that overlap upon the
-pre-Cambrian rocks. Erosion has removed them to a large extent, and
~ south of the Adirondacks the western coast line isunknown. (Fig. 2.)

Po 8

a: ROCKY MOUNTAIN PROVINCE. . P

at:
-- For the purpose of description the area of Cambrian rocks in the

‘ Rocky Mountain Province includes the Cambrian outcrops of northern:

_ and western Utah, Nevada, eastern Idaho, the Gallatin River district
_ of Montana, and the Canadian extension.

% UTAH AND NEVADA.

By; The Cambrian rocks of Utah and Nevada are considered together,
_ owing to their having a common base in the presence of the Olenellus
“zone, the strata of which rests conformably upon a great series of sili-
eeous and arenaceous shales and sandstones, and massive quartzites.
| In Nevada the section is much more complete and reaches a far greater
oe opment both in amount of sedimentation and the presence of
organic remains. The section studied by Messrs. Hague and Walcott
4 in the Eureka district may be considered typical of the Cambrian rocks
of central Nevada. It embraces five formations, all of which are
described by Mr. Arnold Hague in the abstract of his report on —tite
“Geology of the Eureka district.!
_ The Prospect Mountain quartzite that lies at the base of the series
- has a thickness of 1,500 feet on Prospect Peak. It is distinctly bedded
and comformably subjacent to a band of arenaceous shale, in which the

and I am now of the opinion that this should be done, although I have
held the view that the Olenellus zone should be considered the base of
the Cambrian, and the Prospect’ Mountain quartzite I tentatively re-
ferred to an Algonkian formation. The subjacent band of arenaceous
shale is mentioned by Mr. Hague in his report of 1881,? but not in the
more complete description of 1882. In the review of the Eureka section
by Mr. ©. D. Walcott in 1886 this formation is spoken of as follows:
S At the summit of 1 the quartzite becomes more thinly bedded and passes into an
arenaceous shale which is a or less calcareous and, in its extension northward, is

te: splaced by. limestone. This belt of shale and limestone is from 100 to 200 feet in
th hickness and carries numerous fragments of fossils, among which we have determined

TW. S..Geol. Surv., 2d annual report, 1881-’82, 1883, pp. 254-259.
2 Report (on work in Eureka District). U.S. Geol. Surv., 2d Ann. Rep., 1880-’81, p. 29, 1882,
ity ve ag : :

~>

Olenellus fauna occurs. It is referred to the Cambrian by Mr. Hague, ©

eee, = a maf Gre i es a Oe tae NS See. 2 ‘is Cae 5 ieee A Ba gst = ey aa iy : es >a -
hin Po ot eee as Re en eo Serres sae be Sy ae
- w ay a eae Posy ‘ — =<. = a ~ Sore 4 3
Bh Ba,2 5.“ eae THE “CAMBRIAN. SPS tae
ry - Pe = =“ 9
Pee PE species, viz, Kutorgina prospéatonsie: Scenella. Soietii Otenoides quadriceps, Olenellus

res Lapibarlt, 0. iddingsi, Anomocare parvum, and Ptychoparia. ‘sp. Be

- : & > {

The second formation is the Prospect Mountain fiiveabnna Thess - a’

massive limestone erystalline and granular in texture. eerie

Sie ‘Interstratified in the limestone are irregular beds of shale, lentienlas or r wedge |
shaped bodies, varying greatly in width. Indeed they form a characteristic feature — #

- in the limestone, which passes readily from massive to shaly beds. Two of the shale —
__ bands are quite prominent to the north, but are lost to the southward. The thick- 4
; ness of the beds may be taken at 3,050 feet. 2 i‘ a

_- Formation No. 1, the arenaceous shale, between the quartzite and the ze 2
= limestone on Proapacs Peak, is more or less a local formation, but it is
: apparently the zone of Olenellu s, and the limestones above are not —
known to be characterized either by Olenellus or the typical forms of |
that fauna. Five hundred feet above the base of the Prospect Moun- —
tain limestone there occurs in a band of shale Scenella conula, Agnostus

2 interstrictus 2 Olenoides quadriceps, Ptychoparia prospectensis. All but
the last are closely related to species from the upper beds of the Geor- |

gia horizon, in either Vermont or Canada. One other species, Sten-—
otheca elongata, which is found associated with Olenellus thompsoni,
--Protypus senectus, ete:, at L’Anse au Loup, is found 2,000 feet higher go }
in the limestone. Another species, Olenoides spinosus, is found in asso-
ciation with species characteristic of a lower horizon than the typical
Potsdam of Eureka, at Pioche, Nevada.”? 4
Within a short distance of the summit of this limestone the fanna

has the general facies of that of the upper Cambrian or Potsdam hori-

- gon; still as a whole it occupies the position of the middle Cambrian
234 hound as the faunas are now Classified. That it sustains this view was —
- pointed out by Dr. W. C, Brégger, in his admirable paper on the “Age

oe of the Olenellus zone in North America.”*' He compares the fauna of
_ the Prospect Mountain limestone with that of the Paradoxides zone of
Europe and concludes that with the exception of the lowest part of the’
Olenellus zone it must correspond most nearly to the middle and upper

part of the Paradoxides deposits of Scandinavia. His conclusions are
based almost entirely upon the presence of the various species of the a
genus Agnostus. From the results of my studies since 1886, I am pre-
pared to accept this view of Dr Brégger’s and to consider the Pros- |

_ pect Mountain limestone as representing the Middle Cambrian or ge re a

_ doxides zone of the Atlantic Coast Province. A list of ene pa
lished in 1886 is as follows: °®

a

1" ; 1Second contribution to the studies of the Cambrian faunas of North A wacisea: U.S. Geol. Sur ve
Bull. No. 30, 1886, pp. 30, 32. = : e
2Hague, Arnold. Abstract of Report on Geology of the Eureka District, Merada, U. s. Geo!
Surv., 3d\annual report, 1881-82, 1883, p. 255. ~~ ie
3Second Contribution to the studies of the Cambrian faunas of North America, Us; Ss. Geol. Survey,
Bull. No. 30, 1886, p. 32. ae
re 40m alderen af Olezellus zonen i Nordamerica. (On the age of the Olenellus - “Zone ti uae th
f America.) Aftryk ur Geol. Foren. i Stockh. Férhan, No. 101, Bd. 8, 1886, pp. 182-213.
~ 50.58. Geol. Surv., Bull. No. 30, p. 32, : a re

‘ee . “ra Paes et

ee Ss eee - STS RS ee Ee
= : caer: Reis Pe ea ee ; sa eee Pein poh ey ae eee
i ee | By Bie Ae it oe eee
avcort.| SF: "SUMMARY —UTAIT 4 AND ‘NEVADA. <<. Soe ae
; % ~ oe
-g E Seas (like 0. peitioaay _ Protypus distictaa : : =
i -Lingula manticula. — : - expansus. ig
ea" -Kutorgina whitfieldi, Dicellocephalus ? nasutus. :
- Orthis eurekensis. | Ptychoparia oweni. e
_ Stenotheca elongata. © haguei. 2 e
ss Agnostus communis. | occidentalis,
meee bidens. ~~ ~ dissimilis. =
aoa | On. Olenoides spinosus.
3 Rs oe richmondensis.

‘ Of the succeeding: formation, or the Secret Caiion shale, Mr. Hague
says: . --
~The Prospect Mountain limestone passes, by gradual transition, from shaly lime-
at fone into brown and yellow argillaceous shales. * * * In their broadest de-

velopment they measure 1,600 feet, although in places where they are encroached
upon by. the Hamburg limestone they occur considerably thinner.!

- Only: a few scattering fossils are found in the lower portion of the
Bec ecret Cafion shale, but near the summit of the fauna islarge and charac-
; teristic. It pees, Aocordingt to Mr. C. D. Walcott, the following : 32

Re” Protospongia fenestrata, Dicellocephalus richmondensis.

a

i : _Lingulepis maera. Ptychoparia pernasuta, Fa -
Ress. minuta. . laticeps. rade

Lingula? manticula. bella. | ; Te
_--_—.-: [phidea depressa. linnarssoni. -t
-—- Acrotreta gemma. . oweni. Se
_-__ Kutorgina minutissima. haguei. eee
_-_—-— Hyolithes primordialis. — siwilis. a
- Agnostus communis, unisuleata. — ;
oe bidens. — leviceps.

2 neon. . 4 Chariocephalus tumifrons.

’ seclusus. - Ogygia? problematica.

_ Dicellocephalus ? nasutus.

_ of the species in this list Dikelocephalus? nasutus, and D. richmon-
| densis do not belong to the genus Dikelocephalus and the form referred
to Ogygia? problematica represents an undefined genus. Asa whole, as Fast
suggested by Dr. Brégger, this horizon ney possibly be referred to the =a
P aradoxides zone. a5
_ Number 4 of the section, or the Macias limestone, is a dark gray

and granular limestone; surface, weathering rough and ragged; only
s slight traces of bedding. Very few traces of fossils were found in the |
entire 1,200 feet of rocks referred to this formation.

_ No. 5, or the Hamburg shale, resembles the Secret Cafion shale except Ane
a iat it is by no means as uniform in composition, showing very rapid
gle in conditions of deposition and becoming more or less arena-
ceous and calcareous throughout its development as well as in its lateral
extension. Throughout its entire thickness of 350 feet fossils are more -

+ ‘Abstract of Report on Geology of the Eureka District, Nevada. U.S. Geol. Surv., 3d Annual
Re po! rt, ager, 1883, P. 255. 4
Ibid.,) p. 82, , 2

-

>

«

~\

-_. fifteen species pobtinne on into the passage fauna, viz: (species of the Potsdam fauna

+
= -

~ eo

/

~ tena melita, Orthis Rantvere cae O. testudinaria, Triplesia calcifera, Tellinomya <4

nh. oe ae SS > te pene SS pies saet
eet Tey Nceest yene ROR
. re €3 % Pie. & ec

Les pe a

THE CannRTAN. on Noe 3 ae

csbiatied the following g:

a re :
* Thubilepss mera. ziiccilseaplinice Goveama toma: Maa
minuta. marica. — Chas
Lingula? manticula. bilobus.
Obolella discoidea. osceola,
Acrotreta gemma. Ptychoparia affinis.
Kutorgina minutissima. oweni.
Agnostus communis, ~ haguei. .
bidens. - granulosa.
neon. ' simulator.
prolongus. — unisuleata.
tumidosus. breviceps. > °° \
tamifrons. Arethusina americana.
Dicellocephalus? nasutus. Ptychaspis minuta.

“Three of these species, Hyolithes primordialis, Dikelocephalus osceola
and Ptychaspis minuta, are identical with forms from the Potsdam sand-
stone of Wisconsin.” * As a whole the fauna is of the general facies of ©
that of the Potsdam zone of New York and the Mississippi Valley.
This is found in the Hamburg shale, but in the overlying Pogonip lime-. 4
stone there is an assemblage of species that combine both Cambrian |
and Lower Silurian (Ordovician) types. A short distance above, the
fauna is comparable to that of the Calciferous and eek groups of the c
New York section. aS

_The transition from the Cambrian to the Silurian [Ordovician] fauna is very grad-_ ‘
ual, and suck as would occur where there was no marked physical disturbance to in- 4
inénes the faunal change resulting from the natural dying out and development y of f

species or the influx of new species from other areas. : ee

Of the species occurring below the passage beds three are identical with species oc- ;
curring in the Potsdam sandstone of Wisconsin, viz: Hyolithes primordialis, Dicelloce-
phalus osceola, and Ptychaspis minuta ; one, with Acrotreta gemma of the Calciferous 3
formation of Newfoundland; and Pijchaeria oweni is a common species of the Pots-
dani horizon in Montana ait Dakota. These specific identifications and the grea’
development of species of the genera Agnostus, Dicellocephalus, and Ptychoparia i n
the middle and upper portion of the Cambrian section, furnish abundant evidence
upon which to correlate the fauna and the geologic horizon at which it occurs with .
the Potsdam fauna and formation, as was done by Messrs. Hall and Whitfield (Geol. Me.
Expl. Fortieth Par., vol. 4, 1877; p. 199). Ofthe Potsdam fauna eleven genera and

are printed in italics); Lingulepis mera, L. minuta, Lingula? manticula, Discina (sp.
undt.), Acrotreta gemma, Schizambon typicalis, Obolella ambigua, O. discoidea, Lep-

hamburgensis, Agnostus communis; A. bidens, A. neon, Dicellocephalus finalis, D. i ‘in-
expectans, Ptychoparia? annectans, Piychoparia affinis, P. granulosus, P. haguei, ae
oweni, P. unisulcatus, Arethusina americana, Amphion (sp. undt.) Barrandis maccoy visi
IUenurus eurekensis, Asaphus caribouensis. arte
_ In the next superior grouping, about midway of the Pogonip group, all the midal @
Cambrian genera, with the exception of Orthis and Illenurus, have disappeared, and
higher up the genera Receptaculites, Chetetes, Pleurotomaria, Maclurea, Cyphasis,
Bathyurus, and Asaphus carry the fauna up to the summit of the formation where
genera, Receptaculites, Ptilodictya, Chetetes, Strophomena, Orthis, Tellino: m

A Op. eit., p. 33. ie

+ e ~

ml Pe RE ee .
Tig ber Br SEP BS
ee eA. Sie - ,

: = Fg Pat

SP ER ae By OR ee et ee TE oF Ce om ee a
a - ? a eer se ae ats lacs af a : ht SY, ESae
Sei yee A ; te eS ead Ce

» eS were
7 he Aha. ee 3

x Fiemme Js ° : . 1% be
A hy Im, f 7 t cy
* ~ . -

/SUMMARY—UTAH AND NEVADA. 703 I Pe oe
Mod iriajain ae Crytolites, Orthoceras, Endoceras, Coleoprion, Bepiehditia”
Be jrickis Amphion, Ceraurus, and Asaphus give ita facies approaching that of the

z, Lower, Trenton and indicating a horizon that is considered to be in a measure the
ag of that of the Chazy formation of New York and Canada. The fauna of
he lower. portion of the Pogonip group corresponds in‘the same manner to that of
ite Caleiferous sand-rock of the same region. The large number of individuals of

; he species of Receptaculites, R. mammillaris especially,.gives the fauna of the upper
‘ ‘beds a character that this horizon has not hitherto had, This, united with several of
the Trenton species, viz, Orthis testudinaria, O. tricenaria, O. perveta, Tellinomya con-
tracta, two species of Modiolopsis allied to Trenton forms, and Raphisioma nasoni,
8 strongly foreshadows the opening of the Trenton period."

The section of the Highland Range, 125 miles south of the Eureka
asiion, gives a greater variation of sedimentation in the lower portion
and less in the upper as compared withthe Eureka section. The High-
land Range has a more abundant and more varied fauna in the lower
as 500 feet above the quartzite, while in the Eureka section the upper
or Potsdam fauna is much larger than inthe Highland section. In each
instance @ massive limestone has replaced a succession of limestones
and shales. The Highland Range section measuring from the base is as
follows :?

: & ee Feet.
@ Dark reddish brown quartzite, evenly bedded, and ripple-marked in some

‘zg Plac@S ....-. --- 22. 22 ne een eens tee eee eens eens ce eee few ee ck ae
@) Pimehamay limestone ...--.......-- 252-026. -5--- ova kén alg te dlee as naan 35

BS = Fossils: Olenellus gilberti.
8) Buff argillaceous and arenaceous shales, more or less solid near the base

oe and laminated in the upper portions.........<-.--......-.....2-.. 80
_ - Fossils: Annelid trails and fragments of Glenatiasd in the lower part.
4 a4 Higher up the heads of Olenellus gilberti and O. iddingsi occur in
abundance. .
(4) | Lighé-colored gray limestone and bluish black limestone ...............- 16
5) Sandy, Pe -Cotored BHGIO. 2 6 5 8 Soc So ae ce asd cal on con dce esac cess send 40
- Fossils: Annelid trails, Cruziana sp. ?
a (6) Dark bluish black limestone..-...-----...---..+-.- LOR ee t wasnt we aes 46
(7) Finely laminated buff argillaceous shale.........--..----.-..-- REPL may F- 80
iS Fossils : Hyolithes billingsi and Pt, ychopari ia piochensis.
: (8) Gray to bluish black compact limestone ........2..22.022+seseeeeeee eens 18
(9) Buff arenaceous shales. ......--..----.---------- oe er SPR TE ES Se Sy ae Ss oy 64
| mt (10) Compact cherty limestone...--. ..-.--.----- +--022 ++ 222+ eee eee Pete 50
a (11) Compact shaly sandstone in massive layers....--....--..-----.-.-----... 40
(12) Hard siliceous gray limestone, almost quartz at base.... 2.2.22. 2.2-.. 22... 12
. murenmireto ual, Sandy shales... -- 2.5.5. Lewes cadtee see coe caucus ccces 70
a (14) Semeribrelo Vimbeutone 22.2 - 20556202. oso oe elsek bs co apes 16
(15) Yellow-to buff sandy shales.-.. ---. .. 2.2 2..5- Le. cece Win onain aNe oo Ate 40

(16) Bluish black, hard, compact limestone ......---...22.----.-2--2+-20-- rest - 38
- -_- Fragments of fossils. : | 7

¥O% 1) Shaly sandstone in massive layers... sc. 12. sne wee ese eons cone er ccwe cacneee 52
ry as) RP MEUIMCOOUS LIMGRLORO $i cc dace anos ecbnreces suds a nedenaccceedecns 2

: _ 1 Waleott, ©. D.: Paleontology of the Eureka scaabe! U.S. Geol. Surv., Monograph, vol. 8, 1884, 4
Pr 3,4. %

be << alcott, C. D.: Second contribution to the studies of the Cambrian faunas of North America. U.

s - deol Bull. No, 30, 1886, pp. 33, 34.

hte SS

~ . a 2 itt <= Fg 4 ‘bs Pee eS HF Ce Vara” § ent re,
‘ mat 55 Ie : - : fe =e “ = il rh saa ee eae . te * ee Sse we
; : a 4 er in 7 nt ne. fed j 7 . = “eS > Rao * eenaris © <
318 3 EN Pee CAMBRIAN, RAT a ae
; ; “ai 3 : ‘ Fe FR pe — pe - ee ¢ = P. = -" =) “=
: x5 2 a Sit heads t= ae ae co
= “<= > . = +
Cis) (a) Buff, sandy shale. Sic corstesnre teeget - e 40 -
(b) Gray arenaceous limestone aah coe on Sone teenne de sien ememne’n whines 30
(a} Sandy, calcareous shale... -c.as.: isan cecemnues on exes cewene nnn ere

_ row range near the base of the limestone series above the quartzite. _ “a

' (23) Bluish black limestone in massive strata, that break up into shaly layers

0) (a) Massive- bedded, bluish gray limestone... .--- wnt Jab aw aelacusemee ee
Fragments of fossils. ; : z

(6) Compact gray siliceous limestone, almost quartzite in some places 400

(c) Bluish black, evenly bedded limestone.........-..- AP Pre ae! 8

Strike N.30° W., dip. 10° E.

Qh Buff to pinkish argillaceous.shale, with fossils, and a few interbedded lay-—
ers of limestone from 3 to 15 inches thick. ---.-............--.....

Fossils: Hocystites ?? longidactylus, Lingulella ella, Kutorgina pannula, -

Hypolithes billingsi, Ptychoparia jpiochensis, Olenoides typicalis
Bathyuriscus howelli, and B. producta, PaNe

(22) Massive-bedded, siliceous limestone; weathering rough and broken into
great belts, 200 to 300 feet thick, by bands of color in light-gray,
dark-lead to bluish black; on some of the cliff faces the weathered
surface is reddieh: = << 2. toc. Fd co eed SS uy eee Seek pk ewe es ee ee 570

on exposure to the weather. The latter feature is less distinct 850 2
feet up, aud the limestone becomes more siliceous, with occasional
Bhaly’ Hades 3250 ojos etait Seater ok Maman Seok cee Sects 1, 430
Fossils; near the summit specimens were found that are referred to 4
Pt, tychopart ‘ta minor. ;
Quite a fauna occurs in 23,.as found one mile farther south an the line of the sec oer

tion. |
‘ Summary of section. Kove Y;

Feet.
T,, QU arb ibe uns SF Al gsc > Saxd n sae ie BAR Re oea te ae 350
2. Limestone and shales (argillaceous and arenaceous) awaveut 1,450 —
3. Massive limestones ab Wii wattle he Sates pals cate oki aimee giao elanele 000 ,
AS Ree ee eee Ne ee ET EET ey ee ee . 4,800

a
- As in the Eureka section, the species of Olenellus have a very na .

_ The fauna found in No. 21 of the section materially strengthens the
correlation of the fauna of the Prospect Mountain limestone and th e
Secret Cafion shale with that of the Paradoxides zone of the Atlantic
Basin. é Ti
The fauna of the great limestone pelt above 23 of the section is rey \-
resented by only a few specimens on the line of the section. A mile
south, however, on the strike of the strata a strongly marked Upper
Cambrian (Potsdam) fauna occurs. The species identified are us fol-

~ lows: Ete ey pate |
Bellerophon antiquatus. Dicellocephalus sp.? ae
Pleurotomaria, 3 undt. sp... Ptychoparia (Euloma ?) dissimilis-
Hyolithes, 3 n. sp. P. sp.? <
sept pepinensis. _ Arethusina americana...
D. (type of D. minnesotensis). . Illenurus sp.? — oe

Of this fauna two species are identical with those from the higher Potsdam fauna
at Eureka, viz: Plychoparia (£.?) dissimilis and 4r ethusina americana ; and —

bY ’ % 4 >
° < j > 2%.

The p Reese of tlie pishcolovsax(e tis shelis and the species ‘pant mentioned corre-

? nd evada. 1

a We have no details of the section of Silver Peak, Nevada, to which
attention was called by Prof. J. D. Whitney. The fossils are from a
_ limestone and silico- argillaceous shale and identical with species found
lsewhere. The most noteworthy occurrence is that of Archwocyathus =
ES E spirocyathus atlanticus and a large brachiopod like Kutorgina cingulata,
~ both of which occur on the Labrador coast over 3,000 miles to the north-
east on the opposite side of the continent. The abundant and pecul-
iar type of sponge Archwocyathus profundus of the L’Anse au Loup
locality i is represented by the nearly identical species Hthmophyllum
z E ahitneys of Silver Peak, and the tribolite Olenellus gilberti is scarcely
- distinguishable from O. thompsoni, as it occurs in L’Anse au Loup.
‘The species now known from Silver Peak are :?

_Spirocyathus atlanticus. Kutorgina (like K. cingulata).
- Archeocyathus undt. sp. Hyolithes princeps.
ery Ethmophyllum whitneyi. Olenellus gilberti.

_ Strephochetus ? sp.?

~The Cambrian rocks of Utah, as determined by the presence of ine
~ Cambrian fauna, form a narrow herizon in the vast series of sedi-
~ ments of which they are a conformable portion. Messrs. Emmons and
y King refer the 12,000 feet of siliceous slates and quartzites of the Big
~ Cottonwood section. to the Cambrian. If we provisionally drew the
basal line of the Cambrian at the base of the strata known to contain
~ the Olenellus fauna, all but 250 feet of this section would be referred to
_. the Algonkian, but from the known range of Olenellus in the strati-
p Be sriiienly equivalent series to the north in British Columbia, the view

- base a species of Cruziana was found, associated with Olenellus gilberti,
7 5 and 100 feet higher in the section a band of shale afforded Lingulella eila,
- Kutorgina pannula, Hyolithes billingsi, Leperditia argenta, Ptychoparia
- quadrans, and Bathyuriscus producta.. This list was published in 1886,

along with Cruziana and Olenellus gilberti, as characterizing the sisi
at the summit of the great series of quartzites and slates. As in the
- ‘Eureka and Highland Range sections, the Olenellus zone is confined to
a very narrow belt just above the quartzite. The silico-argillaceous
shales above occupy the position of the 4,650 feet of Prospect Mountain
limestone and Secret -Cafion shale of the Eureka section. The Ham-
burg limestone and Hamburg shale of the latter are absent in the
Big Cottonwood section, causing an unconformity by nondeposition.’
- he section in the Géuitch Range above Ophir City has a quartzite at
F the base with shales aboveit carrying Lingulella ella, Olenellus gilberti,
% and Bathyuriscus producta, as determined by the calenieates brought in

* —_ —-
a

i a ee. cit., PP. 35, 36. 2Op. cit., p. 38. Op. cit., p. 39.

la tes the fauna with that of the upper horizon of the Potsdam Fuso of eb nin

_ is no longer tenable. The upper portion of the section consists of 250 ©
feet of hard silico-argillaceous shale, a little sandy in places. At the -

"

SEN Se RS SRC SRE DN pe toro eI INR ee ee
Re ae seri aN ie Goes Ses" OE la koa Nee

J . : . E ; tae te St BNA . -—— < ~ ed SAPP,

} ; 2 ‘ petra ahs oa

320 | ee THE CAMBRIAN. SRY ate [BULL 8h.

section. The section at this locality as measured by Mr. G. K. Gilbert
is as follows:!

that in the former the earlier conditions of sedimentation were appa-—
‘rently the same from the base of the Wasatch Mountains westward —
— into central Nevada. But during the deposition of the Middle and —
Upper Cambrian rocks the immediate vicinity of the Wasatch was an

the deposition of late Middle and Upper Cambrian time in the Wasatch |

logic notes as time permitted. In the vicinity of Malade City, in south- ~
eastern Idaho, he discovered in a limestone resting on a quartzite,

_ by the Wheeler survey. It is probable, Hower, that as in the case of
- the Big Cottonwood section, Olenellus gilberti occurs at the base of the
shale, and the other two species at a higher horizon. At Antelope |
Spring, i in western Utah, there is a considerable development of the
_ Middle Cambrian zone come windind to No. 21 of the Highland Range .
section and a portion of the Prospect Mountain limestone of the Eureka 7

; Feet
1.. Gray, massive limestation: 2-c6 Mas ds ts Bed eacs beer se5ch Oe
2. Blue gray, calcareous shale; fossils (as corrected by C. D. ‘
W.); Acrothele subsidua, Agnostus interstrictus, Olenoides
x nevadensis, Ptychoparia kingi, P. housensis, and Asaphiscus
RONCOLONG x £ «= arin eile, Jah ua ona od wae heehee’ Kens eae eee ae 200
3. Gray limestone, light and dark, chiefly massive..........-. ~ 900
4, Vitreous sandstone, umber-brown on weathered face; base
RO’ SOON. < ca Sols pees cw dpb ead ad hihanl~ See aoe e ener ae ee 1, 000
POLE At cdot pees sReua eta) 8 Wdha fade on phaa pine ot eaten 2, 300

- No. 4 of this section corresponds to the basal quartzite of the Eureka —
and Highland Range section, and No.3 with the Prospect Mountain —
limestone. No. 2 may correspond to the upper portion of the latter —
limestone or to the lower portion of the Secret Cafion shale of the —
Eureka district. There is not enough known of the Antelope Spring
section to enable us to make any closer éorrelation. se

A comparison of the sections of Utah with those of Nevada shows 3

area of minimum deposition, while that of central Nevada was one of
maximum deposition of sediments. What the conditions were during

area are unknown. The appearance of the rocks indicate a shallow .
sea with very little deposition of pevbiatre!s .

IDAHO.

What is known of the Cambrian rocks of Idaho is obtained from the —
writings of Messrs. Bradley and Peale. The report of the former is —
more that of an explorer who, passing over the ground, made such geo- —

fifteen species of trilobites of the genera Conocoryphe, Bathyurus, Di- Y
kelocephalus, Agnostus, ete., five brachiopods, two gasteropods, and —
one pteropod. He referred this fauna to the Quebec group, and the

——————_———————————— ee ee ‘ae

' Report on the geology of portions of Nevada, Utah, California,and Arizona examined in the years a
1871 and 1872. Report on Geog. and Geol. Expl. and Survey west of the 100th merid., in — of
LZ tout. Geo. M. Wheeler, vol. 3, Geology, 1875, p. 167. ih

4 ; ee Ce ty Bs 9 Ae ¥, F rid fi ie tas oe i _ .
is Tine. 3 eek ‘- : em 5 5% Stes ;
“. . SUMMARY—IDAHo. eS ee

tz iti’ Biadscinic beneath is spoken of as occupying the relative
tion of the Potsdam, although he subsequently refers to it as a
part of the true Quebec.! Mr. F.B. Meek agreed with Prof. Bradley
hat the fauna belonged to tiie Quebec horizon; and he? described
Ba ete hiscst) bradleyt and Asaphus éNtenkslaiasts ?) goniocer-
The latter species probably comes from the upper portion of the
lim ius referred to the Quebec group by Prof. Bradley.
om the data obtained by Dr. A. C. Peale of the Gallatin River Cam-
ian, and our more accurate knowledge of the fauna of the Quebec
group, the faunas occurring in the lower portion of the limestone at
Malade City are referred to the Upper Cambrian, and those from the
‘upper portion of the limestone to a portion of the Lower Silurian (Or-
' dovician). In this connection reference should be made by the reader
to Prof. Orestes St. John’s work upon the same beds in Wyoming. |
_ Near the south end of Portneuf Ses. north of Malade City, Dr. A.

C. Peale measured the Aida section :°
= Top. ~

Bi INES gba ee ck. vi soo cs abs Vanes num cpinebace wees seube 130
- Laminated blue limestones, with Conocoryphe, Dikellocephalus,
Obolella, and two species of Bathyurns .................---..- 315
BeEeMIeH GPAY PintestoNes ...5<: 12-2 .- eaenacces cceccecaeccouceee
_ 4, Laminated limestones, with bands of greenish shales i in the upper )
portion. The limestones are separated by shaly layers. The
. _ limestones are fossiliferous at the base, containing quantities
a of a trilobite like Conocoryphe. The limestone resembles an
a oolite, but the structure is probably due to the presence of 120
am some peculiar organic remains. Fragments of Discina were
MNES OW dh Bic ton Sa‘snae os oe EPERT Feit let Peery Bap LLIN aes ees pee
Pe B. Rather massive limestones .... ......--200 -2s- cone cece cece scene .
6. Laminated blue limestones, in bands of from 1 to 2 inches thick-
is ness, the surfaces of which are yellow-stained.
we Rather massive limestones.........-2.----eeees«e aon uty cbaeys
m8. Green shales or slates, 15 feet... 5.2... 22. eee e cece cece e cues 118
9, PPET OM, SETMOBLONG 605 5 05550 i055 558 Sone worse es wes eed s occa cone
x 0. Bluish limestones, with bands of shales.............. 2.222242 eeee 155
‘s s Massive blue limestones. The dip here appears to be about 40°. a0 100
. Laminated limestones with interlaminated green shales ..... eee 70
13. Greenish sandstones and shales, passing below into silvery gray |
te eS Mig a oe hoe af ouccc sxc suc dlawcticetc smee on sigs was 210
14; Slates and shales with a band of limestone about the middle..... 4 185
15. Blue limestones with irregular structure. The strike is about ‘
. south 5° east, and beyond the station it appears to curve to the
IE fhe ess ok nh La cme ewicade tase ace e ol ae8 70
Rusty yellow RNR at oo Phe pmn va buaanbes fn ata oles whan ee - 150
Gray and yellowish quartzites..... PE ree Pe Ee Pe peer ; 450
MN, SeFawepIAtOS 22220... 5 2) Son fed eee akon sa wae eyccere 180
19. Rusty yellow quartzite, somewhat conglomeritic and containing a
we = considerable percentage of iron........ .20. 2. cece ceccee secee : 130
a eos quartzites, about -...--. .. 222. ------ +2220 - cone eee pewculs ss 600
2. Ee Ear e Ee 8 cis wis 5\v. da ees X,ade nie eiecie wale, ajeiv,e ns
2 PermeitenG, witite Guattzited.. 20.0 a... <sobecccuss sceccevecuee ; 500 to 600
3. Red slates, thickness not taken -...........5....... Eodte aioran't See
DM Mi cen A os ab erat ivees Gade ¥e solaceets~ = 3, 483.003; 585

b: ert of Frank H. Bradley, geologist of the Snake River division. U.S. Geol. Surv. of the Terr.,

6th Ann. Rep., 1873, p. 201. -

* _ 2 Preliminary paleontological report; with remarks on the ages of the rocks, etc. U.S. Geol. Surv.

of the Terr. . embracing portions of — Idaho, Wyoming, and Utah, 6th Ann. Rep., Ibid. 1873, pp.
485.

Report on the geology of the Green River District. U.S. Geol. Surv. of the Terr., 11th Ann. Rep.,

a “Bull 81—aL Kee , Z

pce as eee THE CAMBRIAN. ee a
fates 7 = : Pr aen

aS ee Below this last eta there a are © probably, the limestones of the ] Red
tus _- Rock Pass. Sys
‘This section is one of considerable interest, from the fact of its em
“ae _ ing the Upper Cambrian fauna in the upper portion and an alternating —

series of limestones, shales, and quartzites below, which, from acom- —
parison with the sections of western Utah and central. Weveda occupy —
the stratigraphic position of the Middle Cambrian. In their downward -
. eontinuation, they may also include the Lower Cambrian zone. This :
ig a question which is to be settled by future investigation. a
-_ _In the adjoining Bannock range to the west, Dr. Peale studied a section E

of the series of quartzites and slates that sonaevulle correspond to those .

: _ of Nevada and Utah, occurring beneath the Lower Cambrian (Olenellus) |
gone. The section figured by Dr. Peale includes 5,710 feet of quartzites —
. -and slates, with a little interbedded limestone. He compares it with —
the section on the western side of the Wasatch range, referred to the
Cambrian by Messrs. Emmons and.Hague.! In his résumé of the for-
mations, the Cambrian or Primordial is made to include the quartzites-
and slates that may be tentatively assigned to the Algonkian, or to the
Cambrian, but preferably to the latter. To the Canadian Period there
are referred 1,300 feet of interlaminated limestones and quartzites that
occur above the quartzite and slate series now referred to the Cabri
Dr. Peale states that west ef Malade City the section gives 2 sp00 feet
of strata placed in the Quebec series by Prof. Bradley.’
: The northern end of the Port Neuf range was studied by Prof. Oreste Ss
TE St. John, in the vicinity of Mount Putnam. He there found the section 12
ax to be nad of quartzites, chloritic schists, slates, and micaceous shales :
at the base, above which comes the dark red, finely laminated san
stone in thick beds. These he referred to the Saletan with a query
In speaking of this section, Dr. Peale says he thinks Prof. St. Sohn is

| inclined to refer the base of the section to the Huronian.? —
Hes With the information afforded by his own survey and that of Prof 7
_ §t. John, Dr. Peale constructed the following table as embodying their r

=: spiwilea of the Lower Paleozoic section of Idaho : 4

1 Op. cit., p. 570. 2 Op. cit., p. 614. * Op. cit., p. 615. _ 7 ‘Op. cit., p. 615. Ey

ee

a =<"
~ SUMMARY—MONTANA. -
‘ ~ Siluri an sshabtiar:

-

Blue and gray limestones, with characteristic
Quebec fossils,

~

tion 133.

Blue limestones, generally laminated, with al-
ternations of greenish saudstones and shales
and siliceous slates

1,500 + ft

ous?

- "
1 \ 4 , a, Fi tet ‘ aah oie « ;
¢ " 4 : igns ; _
| ” ; z ae Parcs
‘ 3 os . - ae a by
‘ ’ . A ay : ; Dae oe,
; : ‘ ae aS | eat Ty | “~ n
; ) 4 7 re cat + hall
‘ é < es ot és Y Ws
MN A h
‘ : : a 2
3 ; i ab 7: hea, 5
' 4 a i Or. $ a.
— = - — ry wa 9
: " 1 ‘i ee ee
‘ vs ee
p * as . : .
\ - + Va we
\ , *
. z J “ J y , we
y ‘ J i : at 4 ae) ty"
- 7 t« Pas Fr.)
4 t tas .' +
‘ ‘ « y g a ye
- 3 Bs 7 s
ee & Pon fe
d J Te: ine
. , 28 a
. — a: -
AR
. . . - [ “vy :
= : id . >
y ae
‘ z
2
: bbe wit
.
wl é
,
g . Me 6 s
\ 0 !
cd ‘ %
i P - ae
Pg eg
i be
J on
‘ : Wy
i ay \ nls
: 7 ia
os,
’ my! }
. pn @
? 1
bd _ st
. J
nd '
a
A 7 * <a
b Be
“ - ; aa
‘ .
.
;
’ e >
. ‘ 4.
* ‘
4 .
. . -
‘
! ‘ 12
a .
: ’ 5 ey
. > . ttt! Sy
: le
he i"
{ :
t . x
ie Ae
: ‘ “
ji te
-
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/>
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‘ +’
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‘ « ,
Section No. 21, st ek
- a
ection, No. 21, sta 2.
. . Pye
¥
: 4 ! e <

Calcifer-
500 ft

tt. | 1,000-+ ft

~*~

g | 8s z #
‘Foe ES Pink and white quartzites, conglomeritic at | +
2 |'g % top, with thin layer of limestone at the base. | ©
= 7) a site = ie ‘
x m [Os of a
me | re 8 :
“ees Olive green aad gray chloritic slates and in- | J : =
«ides durated clay slates. eo, 8 i :
eae’ az tf ay ee
“ren pe 3 : > 5 S 3 *
Asa | is eal a 4
der 3 & | Silvery and steel-gray micaccous slates. |e | a ef
a - 7 L a
Pe hg | 4 es 3 ie.
= & : af g we ae
a on} R Ve
ars =) ? e - ay
, # ee Dark quartzites with interlaminated slates. S :&
; mg 4. a 204
; 2 mo kf %
oe, 8 \ as
ee Se | Rea quartzites ee quartzitic sandstones, with con- be) :
SS = glomeritic and shaly layers. Ze =
a ee oh 2 = ae
a Limestones. & a
ao m | &
—- Bm Qn ra)
a | Very Saks green chloritic schists, containing quartz | _. - Ai ;
a and serpentine seams and interlaminated bands of | & =
< metamorphosed argillaceous slates, anda band of | S&S =
pink ere 200 feet thick. a 2
<a)
In copying the table it has been reversed, so as to follow the nat- |
Ee iral order. As interpreted in the light of our present knowledge of
_ the Cambrian rocks in the Rocky Mountains, the Quebee and Calcifer-
ous of this section are referred to the Upper Cambrian. Whether the
_ rocks referred to the Potsdam and Acadian are of Cambrian age or not
— will remain undetermined until some paleontologic proof. is obtained. :
el MONTANA, ne: ee
& As far as known, the Cambrian rocks of Montana are restricted to the
~ southern portion of the State. Twoareas are well defined, one about
eS the northern end of the Big Horn range and the other wikia the area
| drained by the Gallatin and the Yellowstone Rivers. :
Se; th be Lak af x z = ~

> S f { > re Sans ey vs - aes et
g ; i = n pte et: a ae: ak sg : Aes
: - ‘ . . eal ats site Ge
ad “324 Ams Ete sa THE ‘CAMBRIA. ee Lee, (BULL. 4
. fe Pate 8

~The shamaetee af the strata orale g the Cambrian ieGat the Big Horn f

“Mountains will be spoken of in connection with the extension of that |

- range in Wyoming. The Gallatin section of the Cambrian includes.

_ 1,250 feet of strata, of which 835 feet are limestone, resting upon 415 A

feet of sandstone. Conformably subjacent to the latter, there are 5,000 —

- feet of alternations of conglomeritic, micaceous sandstones, with bands — “aq

of siliceous limestones and indurated clay shales, referred. to the Algon- —

| kian by Dr. A. C. Peale.? q
A more detailed manuscript section, that Dr. Peale kindly prepared —

at my request, Is as follows:

Ne { Pebbly limestones 145 foet.
(fossils, Leptena melita, Ophileta sp.?
Triplesia calcifera, Ptychoparia sp. ?
. Ptychoparia (£.) affinis).
: Dry Creek shales 30 feet. _
Mottled limestones 160 feet. ;
(fossils, Ptychoparia sp.? Hyolithes sp. ?)
Gallatin limestones 835 feet... { Obolella shales 280 feet.
. (fossils, Obolella sp. ?) j
Trilobite limestones 120 feet. | use
‘fossils, Lingulella sp., Acrotreta gemma. ae
Kutorgina sculptilis, Agnostus bidens.
Hyolithes gregaria, Olenoides serratus.
Ptychoparia gallatinenses.
Bathyuriscus? haydeni).-
. Gallatin shales 290 feet. a
Gallatin sandstones 415 feet. -- (fossils, Pan eae S y olithes sp. : a
Gallatin quartzite 125 feet.

It is probable that the 5 000 feet of strata referred 6 the Aloonkciain q
in the published section will ultimately be referred to the Lower Cam-—
_ brian as they occupy the stratigraphic position of the Bow River series _
to the north in British Columbia through the upper 3,000 feet of which=
the Olenellus fauna has been found to range.
The section near the mouth of the East Gallatin River was studied
in detail by Dr. Peale in 1884, and two lithologically well defined groups
determined and cinsraciorsaed as follows:

<__

To the lower one, which was carefully searched, without success, for organic re- S !

~ mains, the name of East Gallatin group has been provisionally applied. It is com-— 3

- posed of a series of alternations of green and greenish gray micaceous sandstones and —

clay slates (almost argillites), with thin bands of laminated limestones; 2,300 feet of
these beds were sectionalized in detail without any traces of fossils pele found,

The sandstones are in heavy beds and present a somber appearance, weathering on.
exposed surfaces to steel-gray and almost black colors and frequently breaking into . t
cubical blocks. The slates are blue, yellowish, olive-green, and at some places red.

is In the limestone a concretionary structure is frequently noticed. For the upper a
group, lying above a well defined pink quartzitic sandstone, we have retained the — Ey.
name Potsdam. Green and dark purplish red micaceous shales, mostly arenaceous, — 4

-_-with occasional thin bands of limestone, make up this group, and many of the beds |

- are highly fossiliferous. The collections have not been carefully studied yet, and we | a
therefore simply refer to them in this general way at this time.? / .

1 Report of Dr. A.C. Peale (on the Montana divizion of geology). U. S. Geol. Surv., 10th vi
2. $800, p. 13h. + oe
a bape F, V.: Report Montana Division, U.S. Geol. Surv., 6th Ann. Rep., 1884-’85, ae 50, .

s - ‘
* - ‘4

re ed - Tie pees fee ate
: eee cS ted tae Re Oe ar eee =
~ 4 i> 1?» SUA ve bed pat - 4 7
wa 2 ee _ SUMMARY—MONTANA. | 825
a= et >

! 4 872 was studied by Mr. Meek, who recognized eighteen species. From
he lowest division he identified the genera Cruziana, Lingulepis, or
Ser ioke, Conocoryphe, Bathyurus, or Asaphus. From the third divi-
4 sion he described Bathyurus serratus, B.? haydeni, Conocoryphe (Con-
; ~ ocephalites) gallatinensis, Iphidea subtilis, and Agnostus bidens ; and iden-
tified a species of Conocoryphe, Hyolithes gregaria, and Acrotreta sub-
conica. From the second division the genera Acrotreta and Lingula
are identified, and from the upper or first division Asaphus ?, Bathyu-

the Upper Cambrian zone, although that of the fourth or lowest di-
-. vision may prove to belong to the Middle Cambrian. As a whole the

_ above which occur limestones carrying a fauna characteristic of the
upper portion of the group. 2 .

_ The presence of the Upper Cambrian on the southwestern side of the
“Little Belt Mountains and on the southern side of the Elk Range was
proved by Messrs. Dana and Grinnell when they discovered fossils of
‘thisage. The section near Camp Baker, southwest of the Little Belt
- Mountains is estimated as follows :?

- Quartzite, 20 feet; variegated shales, mostly bright red, also green and blue, 150
BF soci: limestone in a double series of ledges, 80 feet ; quartzite, reddish, slightly mica-
cosine, then a series of colored slates, mostly green, “lowed by shales and thin beds
os sandstones and limestones, in all probability 1,500 feet ; still further conformable
shales, 1,000 feet. These extend toward the north farther than we could follow
them. It is enough to say that the total thickness of the conformable strata under-
lying the fossil-bearing limestone can not be less than 3,000 feet, and is probably
much more. ;

The same authors state that they identified similar rocks at Moss
Bi rsts Springs, at the south extremity of the Elk Range of mountains.
_ The strata there are red shales, quartzites, and limestones like those at
ae Baker, the limestones containing many fragments of trilobites.
The fossils collected were studied by Prof. R. P. Whitfield, who de-
~ seribed Crepicephalus (Loganellus) montanensis and Arionellus tripune-
tatus, species that occur in the Upper Cambrian horizon, the former in
the Black Hills and Big Horn Range, and the latter in dential Texas.
a _ From his observations at numerous points Dr. F. V. Hayden con.
_ cluded that the outcrop of the sandstone referred by him to the Pots-
dam extended entirely around the Big Horn Mountain Range. Near

pe Carboniferous limestone, resting unconformably upon the schistose
and clay slates of the Agoic series in very nearly the same manner as

‘-

ce. Reh. paleontological report . . . with remarks on the ages of the rocks, etc. U.S.
- Geol. Surv. of the Terr., 6th Ann. Rep., 1873, pp. 463, 464.
__ *Geological report. Report of a geological reconnoissance from Carroll, Montana Terr., on the

"a Upper Missouri to the Yellowstone Park and return, made in the summer of 1875, by Wm. Ludlow.
1876, p. 133,
-* Descriptions = new species of fossils. Ibid. p. 141.

ae :

©
ey
4

y

ied : e ;
ie oe ae “es
we ool eS -

» t “> > —,

a ~The: Ratios toll Sated | in the Gallatin River section by Dr. Hayden in —

rus? Conocoryphe, and Lingulepis.!. This fauna has the Hele of |

Cambrian of the Gallatin region is formed of a sandstone at the base, —

the sources of Powder River he found a series of sandstones underlying.

i

al ee ee ne sieve ar Sy ven SS: eI ape AES Oe ee ee ae :
> oo a ar" 3: r ee ee oe * ase o Cary “= $e ay ~e fot toe ne tw ee
fe , Ke OO p ; P< . ee Pe ieee a ee Se Ro > = oe
2 Pp a t : © = = - an aS. - i C- Sa
a : n e - Ny ar - * +s mat BK i ~ Oe ae, Ie a ie nF ¥ a
3 F od wee: : : oF a ee he 3 Phe Dye ry Se er
c . ‘ e, ara, tPA? -#3 ‘ “a
326° ter eee “THE CAMBRIAN. eg a ee (BULL. 81,
. : —_ <—s rr)

: = inch in diameter, cemented by siliceous matter. Above, the rock is in

~~ The Cambrian section, identified by fossils, includes the upper por- —

_ and frequently grade into flaggy sandstones that are often slightly cal- _

_ and occur in thick, massive looking bands, alternating with quartzites

a , —e ab &,

in the Black Hills. The Potsdam saudstone} in thie’ region is a quits well
developed, attaining a thickness of 200 feet, and exhibiting, as usual, 4
various lithologic characters. Near the base, the rock is of a reddist >
flesh color, very compact, composed of an aggregation of quartz peb-
bles, varying in size from a minute grain of quartz to masses half an —

thin ferruginous layers, slightly calcareous but mostly siliceous, and —
, - with many small particles of mica. These thin layers are also charged
with fossils, such as Lingula antiqua, Obolella nana, Theca gregaria, and —
~ Arionellus ? ? owent. Many of the slabs are covered with fucoidal mark- ©
ings and what appear to be tracks and trails of worms.!

2

a a

CANADIAN EXTENSION.

- Our knowledge of the Cambrian rocks of this region is mainly limited
to the vicinity of the line of exploration across the Rocky Mountains i in
the vicinity of the Canadian Pacific Railway. They occur in western —
Alberta and eastern British Columbia, as is shown in the plates and —
sections accompanying Mr. R. G. McConnell’s paper.? The geographic — “4
distribution and the localities mentioned by Mr. McConnell are repre-
sented on the map accompanying the report of the Geological Survey a
of Canada for 1882. 4

tion of the Bow River group and the lower part of the Castle Mountain —
group. The Bow River group forms the basal member of the section in a
the Bow River Valley and Cathedral Mountains. It consists mainly of
a series of dark colored argillites, associated with some sandstones, —
quartzites, and conglomerates. The argillites are usually dark grayish
in color, but become greenish and purplish in places ; are very impure, — =

_careous. The conglomerates of this series are characterized by pebbles :
of milky or semitransparent quartz, and by pieces, similar in size and
fresh looking, of whitish feldspar, and the matrix contains an abundance ” ay
of pale mica. These constituents have evidently been derived from —
some not far distant exposures of coarse granite or gneissic rock. ‘The :

conglomerates characterize more especially the top of the formation, —

and shales. The quartzites, like the conglomerates, are mostly found —

in the upper part of the formation, and sometimes, as in Cathedral _ x
_ Mountains, replace the latter altogether. The only fossils detected in — a
the Bow River series are specimens of Olenellus gilberti, found about
2,000 feet nro the top of the formation and at the summit of Vermilion —
ey

4The Primordial Sandstone of the Rocky Mountains in the Northwestern Territories of the United

States. Am. Jou’. Sci., 2d ser., vol. 33, 1862, pp. 71, 72. 4
5 Report on the Geological Structure of a portion of the Rocky Monntéing, with a section. Geol. Gr

Surv. Canada, new ser., vol. 2, 1886-87, pp. 24D-30D.

eh Pore a ae ee ar
aes ; ae om “as 35a

_ SUMMARY—CANADIAN ‘EX'TENSION. gk Ae

BA ttention was called to the resemblance of the strata of the Bow
S River” series to those of the Big Cottonwood Cafion section of the ~~
~ Wasatch Mountains of Utah, by Dr. G. M, Dawson, in 1885. Acom- =|
parison of the two leads to their correlatiun as equivalent formations,
on the evidence of their lithologic characters and stratigraphic position
and the fact that the Olenellus fauna occurs in the upper portion of
& ee Pectin: In his paper of 1889 Mr. R. G. McConnell! states that
_ specimens of Paradoxides and other fossils were found at the junction
E of the Bow River and the superjacent Castle Mountain group. A col-
lection made at this horizon was sent to me for examination, and I
4 identified Olenellus sp. undt., Protypus senectus, and a species of Ptychop-
. aria undistinguishable from P. adamsi of the Olenellus zone of Vermont.
q __ The occurrence of the Olenellus fauna at this horizon and of Olenellus
- gilberti, 3,000 feet lower in the section, corresponds to the great range
ay at the pita in the New York and Vermont sections.

The Castle Mountain group, in the Castle Mountain section, com-
~ mences with a thin band of shaly limestone, above which come 1,500
feet of massive dolomites. These are subjacent to some yellomsia,
a Deiat, impure dolomites, above which 300 feet of reddish shales oc-
- cur subjacent to several hundred feet of shaly magnesian limestones.
~The Mount Stephen section shows about 5,000 feet of beds, consisting
mainly of heavy dolomites, with shaly bands at intervals. One of these,
oceurring at the base of the formation and another about 2,000 feet —

Ey - Bete, up, are rich in trilobites.” = =
+ _ Reference has already been made to the fauna occurring at the base
3 of Castle Mountain. From the next fossiliferous zone, 2,000 feet up in
- the section, the following species have been obtained : Fs

«

,

x -Lingulella macconnelli. Agnostus interstrictus.
Crania? columbiana. Olenoides nevadensis.
og Kutorgina prospectensis, Zacanthoides spinosus,
oe _ Acrotreta gemma, var. depressa. Ptychoparia cordillera.
a oo Linnarsonuia sagittalis. Bathyuriscus howelli.
~—~——s Orthisina alberta. (K.) dawsoni.
ae Platyceras romingeri.. Karlia stephenensis.
= Hyolithellus micans. : Ogygopsis klotzi.
a - Where the line between the Cambrian and the Lower Silurian (Ordo-

— vician) is to be drawn in the Castle Mountain group is still undeter-
mined. The discovery of a specimen of Ptychoparia oweni in the
Be ebris washed down by the Cascade River from the Cascade Mountains

_ indicates the presence of the Upper Cambrian fauna in this region, and
y itis not improbable that it will be found in the Castle Mountain or
_ Mount Stephen section.

SR TS EES RS Pa ac Oe a EE
1 Notes on the seology of Mount Stephen, British Columbia. American Geologist, vol. 3, 1889, pp.
22-25,

‘ . E- 2 Report on the Geological Structure of a portion of the Rocky Mountains, with a section. Geol
— Surv. Canada, new ser. 1886-87, 1887, pp. 24-29D,

=)

;

eG Se

ae The sedimentation of the western area is much more varied and |
larger than that of the eastern side of the Rocky Mountains. The a

“@

and Upper Cambrian. The Lower Cambrian fauna is well developed —

a

Py an, ! ete Bi ty eat Mater 7. cal fp SNe ~ OV Pat od OE, ON) ea es
ay ere wre zou ie bas 27 pat aie ane aN eke ef haat Sie bea i haa at oy

_ a very deep sea without deposition of sediment, during the latter Pate

upon the shales of the Cambrian, without any apparent unconformity. | &

= - ve Fi
» “ie a Pi . 4 4
4* re ‘ te Pi) 4 a ee ee, - ; ™)
Fan ea ane a ne xe Ft Aina Be sh = Re hs Ne ged) ; Pm te eM, *
: Ng Soa SP es aa 8 ae ae
a

» “a >
Lie .

RESUME, wakit 4 CGT a a

southern portion, represented by the Eureka District section, extend. — _
ing from the basal quartzite to the base of the Lower Silurian (Ontovi
cian), is a continuous conformable succession of limestones and cal-
eareous shales, with the exception of a narrow belt of arenaceous —
shales resting directly upon the lower quartzite. The calcareous sedi-
ments are 6,200 feet in thickness and include the faunas of the Middle_ =

in the shales between the limestone and the quartzite. The Highland a
Range section, 125 miles to the south, has a thickness of 4,800 feet of —
limestone, between the quartzite and the Lower Silurian (Ordovician). P
Proceeding eastward from central Nevada to northern central Utah, oY
the Cambrian formations thin out, and on the Hanks of the Wasatch —
-Mountains are represented by 250 feet of argillaceous and siliceous — 3
shales above the basal quartzite. In this section only the Lower and q
Middle Cambrian faunas are found. The three thousand or move feet
_ of limestone, with an abundant Upper Cambrian fauna, found in central 4
Nevada, is unrepresented. 3
A comparison of the section in the Wasateh Mouhtatns with that of —
Nevada shows that in both the earlier conditions of sedimentation — a
were apparently the same. But during the deposition of the Upper —
and Middle Cambrian rocks, in the immediate vicinity of the Wasatch © Ly
Range, it was an area of minimum deposition of argillaceous sediment, i
while that of Central Nevada was one of a great accumulation of calea- =
reous sediment. a

What the conditions were in the vicinity of the Wasatch Range —
during the deposition of the great calcareous deposits of central Nevada —
of Upper and Middle Cambrian times is largely conjectural. The :
physical appearance of the rocks indicates a shallow sea with very —
little deposition of sediment during the earlier portion of Sra
time, and either a very shallow sea without deposition of sediment or ag

of Cambrian time. It may be that some sediment was deposited and —
subsequently was removed by erosion, but this is exceedingly doubtful.
The pure limestones of-the Lower Siturings (Ordovician) rest. directly =
f

To the north, near Malade City, Idaho, there are 1,200 to 1,400 feet — ’
of limestones that occur above the series of quartzites and atone The —
sedimentation is essentially the same as that of central Nevada wish —
the exception of a less amount of calcareous sediment above the basal -
quartzite. The Upper Cambrian fauna has been found, but not the
Middle or Lower fauna. Still farther to the north, in western pete oe
and eastern British Columbia, the same seriesis represented in the Bow —

4

y"
Le cae ee
-

sommary—rooky MOUNTAIN PROVINCE. ns ee

ver quartzites ‘and slates. “The Oainbrian aloe at this point also
ees closely with that of Nevada. The Olenellus fauna occurs at the
a Ase ofa thick series of limestone, and in caleareous shales, 2,000 feet
I 1igher up, the Middle Cambrian fauna is well developed. Where the
line between the Cambrian and Lower Silurian (Ordovician) is to be
drawn i in this great series of limestone and calcareous shales is still un-
determined.

— r t
a, ul 2
rig

a
ma

Ma em gh
ne
| British: Colombia.

7 a
hes |

ee

be
* = ee & 4
‘ es a 5

i a a 2 .Q,

,, Bee
oo Ses ‘

7 < Sos coe | ge
= ee \ \ ‘

. oa =| SR DL.C. MC,

ae S&S eh | ee 8
Ethic \ 5
a ve ta
. ys gh \

. === 5 | an 3 S

S = » | Ba :
EM.” BG = ates ey

7 ee ee
= Sets 2 vy 8
ot ‘ “y sy =
Ss ra aoe ae eo
Rr: ey a a et
v =a
‘SS ‘

Bi ———— *
— SS L.C.?
* St re Sivas
— I eS

= : "Seana
a es

x : os
-s oy Poh
as SS aus
ie. ia
"= === as

Fs re
“3
i 18 16

a Fic. 3.—Sections of the Rocky Mountain province, vertical scale 6,400 feet to the inch. The num-

ber Lean ees each section corresponds to the locality number on Pls. I and 1. .

= The presence of Olenellus gilberti 3,000 feet down in the Bow River
"quartzite and shales gives strong reason for referring the entire Bow
River, Idaho, Wasatch, and Nevada quartzite and shales series to the
_ Lower Cambrian. We know that the vertical range of the fauna is
- great in the Appalachian sections and also in British Columbia.

2 As a whole the sedimentation in the vicinity of the shore line of
Utah was limited in amount in later Cambrian time, and consisted
- mainly of siliceous and argillaceous muds. In the deeper sea to the
_ westward a great accumulation of calcareous sediment rests upon the
x asal quartzite, and this continues to southern central Nevada. To
the northward there is a decrease in thickness of the limestones across

‘daho. In British Columbia the section is more like that of central
Nevada.

PGR OPES TR Leh ete Tie Micke ee ae

4 Sng , nan AGH t= cok
aa ae . , uy 4 mn ac > bY
ig % i + MG: of pout 7 t ‘ :

4 "ee

a _ where it passes into Minnesota on the northwest. Its line of conte ret b

-»

~

early Cambrian time, and a relatively rapid depression at the begin:

- der or Adirondack sub-Province, the western border or Rocky Moun-

~ ered best to speak of them collectively. a

- accumulation of sand. The rocks are mainly light-colored sandstone

FO Ps a a a AS ee pai. Tig Mies ees be tae Sys
a Rw eater ee eee esse a ti cee PER ge iS yap ce
x es wv > Sip (Gen, ee am E a ore
P a ee oe mS ¥. ° * ae t prix 5

+S aye ~ ~~ * ‘ ica = < ae
bs Zz - : 4 - * <> ae ts oa

Bt Yael =o Bs i, oo ea ~ Cas, a} tie ZT, BE pe hr tee ©
830 = Pee ee ban THE: CAMBRIAN. ab ee oa

PS Be ta ee ee ae ea

A comparison of the seciona of the area on the ‘eastern ‘gine: of 1
"Rocky Mountains with that of the. western sustain: s the view that di

eastern Rocky Mountains and the ick tha to the cantata were above ve
the sea level, whilst to the west the sediments of the later Algonkian 4 2,
~ Lower ee and Middle Cambrian were accumulating west of th d
line of the Wasatch Mountains and the extension of this line near} ly
due north into British Columbia. Over all this region the coast line
and sea bed appear to have undergone a gradual depression during q

ning of Middle Cambrian time. (Fig. 3.)

THE INTERIOR CONTINENTAL PROVINCE.

4
” ae
:.

This province includes the Upper Mississippi area; the eastern bor-

tain sub-Province, and the Llano County area of central Texas
the Grand Caifion of Arizona as a minor southwestern sub- Province, — d

The Lake Superior sandstones and the controversy in relation to
them will be noticed under a separate heading, after the description o R
the recognized Upper Cambrian rocks of Wisconsin, lowa,. and Min-
nesota and their Canadian extension.

UPPER MISSISSIPPI VALLEY.

ot the historical review the literature pertaining = these rocks has S.
been considered under the headings of *‘ Wisconsin,” ‘‘ Minnesota,” and
‘‘ lowa,” but as the strata all belong to one geologic basin it is consid- |

The formations that have been correlated with the Potsdam sand-
stone of New York will be treated of under two headings: (1) The
St. Croix or ‘¢ Potsdam” sandstone proper, and (2) the sandstone ¢ of
the south shore of Lake Superior. ‘9 a

The St. Croix (‘ Potsdam”) sandstone.—The greater sermon of the ex.
posures of the St. Croix or Lower sandstone occurs in Wisconsin, and it
here also presents many variations in sedimentation and fauna. ls iS
lower beds rest on the great pre-Cambrian nucleus of the center of t
“State, extending about it from the Michigan line on the northeast

with the superjacent Magnesian limestone is also very extended owi
_ to the numerous streams that have cut through the limestone down i ep
the sandstone throughout its line of outcrop. The epoch was one 01

in centraland southern Wisconsin, but embrace some beds of wap one e
and shale. The maximum known thickness i is about, 1, ,000 feet. ¢

CN igh i Hie a a Eg a ae lh a I al oY a Ae
hie? Fe * 4 in SO te é we a ae are PN ed Sei? — x eo
Se S eo. a1 eS ors GREE = Poh NC Ra Ys ee
Oe , *> 3 ; > = Pe = o> = = F .
WALCorT.] eS _ SUMMARY—UPPER ‘MISSISSIPPI VALLEY. ~ — 331
% oe at

OAR = - $F
de 5 oak f

DSi the paki n side of the ai vohede Island the lower part of the formation usually
Saatote of coarse quartzose sand, of an exceedingly open, porous nature, with but
“little aluminous or ferruginous and almost no calcareous matter. Higher in the
series the sandstone becomes finer grained and the accessory substances named more
Beiindonit: Somewhat above the middle of the series a a stratum of shale occurs, at-
>t: ining a known thickness of 80 feet. This is not everywhere present and seems to
be mainly developed at some distance from the ancient shore line. It appears to
= ‘indicate that for a time there was a deepening of the waters, admitting of the accu-
m ulation of fine sediment, except near the shore, where the deposit of sand continued.
Above the shale the sandstone, reaching a thickness of 150 feet, is again found. This
z is medium or coarse-grained and slightly calcareous. It, in turn, is overlain by a
+ deposit of associated shale and limestone (the Mendota Hsiieaioaes: which attains a

“beds indicate a modification of the conditions of deposition, such as to permit not
or ly the settling of fine sediment, but the accumulation of calcareous mud as well.
J he latter was doubtless derived from the calcareous remains of life, since the sea
then swarmed with living organisms whose shells and skeletons are found entombed

portion were ground to powder, forming the calcareous flour that subsequently hard-

ing of the waters.

- Overlying this impure limestone is a third and thinner bed of sandstone (the Madi-
oi) with which the Potsdam series closes. This, on the whole, is finer grained than
‘ hat below, and is bound more firmly together by cementing material, which is
2 nainly a calcareous and ferruginous infiltration. The thickness of this bed is about
30 feet.

a In eastern Wisconsin the formation is divided by Prof. Chamberlain
§ into. six parts, as follows, beginning at the top:

Feet
Sandstone (Badison) 625-2 cence se cee cone se ecew cee iat didn we 35
Limestone, shale, and sandstone (Mendota)......... pilerswahingion bee 60

UREN, GUIORTOOUS «os aide cone coupes ben wacrndlebescccns-nive 155
Bluish shale, calcareous .........+...-- bead ts ACINe Sia oo 5 Sade 80
pamas.one, Slightly Calcaroons. 2.2.2.5 200. 2.cc6 wae eee ncn nee one 160
Very coarse sandstone, noncaleareous ........---..------------ 280

a

_ they grow less toward the northeast. Where the total thickness of the formation is
‘reduced by the inequalities of its Archean bottom it is by the loss of the lower
members of the group and not by the thinning of all.?

- The Upper or Madison sandstone is described as a rather coarse-
rc grained, thick-bedded, compact, but soft, slightly calcareous, light-col-
-ored Rertaboie. In of upper portion, immediately beneath the lower
_ Magnesian limestone, it is at most localities coarse, and the topmost
ke ayer is often broken up and mixed with calcareous material, giving it
€ -acoarsely brecciated structure. The subjacent limestone (Mendota) con-
sists of a group of alternating strata of arenaceous magnesian lime-
stone, sandy calcareous shales, and shaly and calcareous sandstones.!

1 General Geology. Historical Geology. Paleozoic Era. Geology of Wisconsin. Survey of 1873-79,
Vol. 1, 1883, pp. 121, 122. -

con n, Survey of 1873-’79, vol. 2, 1877, pp. 259, 260.
ry “0p. cit. 1 P- 260, =

nad oa

thickness of 35 feet in the vicinity of the lake from which it derives its name. These

ii n the strata. -The frequency of broken and worn fragments implies that the greater _

# ped into limestone. These beds appear to point quite surely to a moderate deepen-

_ The thicknesses- given are subject to considerable variation. Asa general rule ~

BE rocclogy of "eastern Wisconsin.] Chapters7 and 8. Lower and Upper Silurian. Geology of Wis-

Pa Salon Ea Coes SoG ee ee

2 . 7
- - . : 7°

SOO ee eee tes “THE CAMBRIAN. Dos pitgat ses eee

ne ; ie. t

‘The upper and«lower limits of the mi Sati group are scarcely def
| able. “It graduates above into Madison sandstone, so as to nickel
. difficult to draw a line between the two, and below the alteration ;
-. -ealeareous and arenaceous rock make it equally difficult to say where e
the series ends. The Mendota beds are regarded as the eastern equiv-
—_ alents of Dr. Owen’s Fifth Trilobite bed, the common horizon being

characterized by the presence of Dikelocephalus minnesotensis, D. pepin-

ensis, Lingula aurora, L. mosia, and a few other species of limited hori-

~~ zontal distribution. The lower divisions constitute the main body of the
Potsdam sandstone and present but very few exposures in this region. ne 7
; They are divided into four parts.}

The strata referred to the Potsdam sandstone by Prof. R. D. Irving
in central Wisconsin have a surface distribution of over 6,000 square
miles.? In the vicinity of Madison the following iain of layer
between the Mendota base ra the Archean occurs :?

ia at

Feet.
4. Greensand hiyot.isscien dh ytesccoddensac S Ma kiks inc ie ix BA 1
2. Calcareous and polomttiR, friable, fine-grained, greenish sand-
? stereo: cae ee eR ae ae Pit Page gt aS
; 3. Not known........- bbs Sei nee Meeks ee aloe Cc oN ae oee eam 31
~ 4. Light colored sandstone, for the most part purely siliceous,
eet being made of rolled quartz grains; but no specimens ob-
ee tained from the i ht on ioe area Sinks past Mae 704
7 5. Red shale..... b Stak nanos db Gr coined whee kee tae dienes a
Total..c.q. 2s ster weaat ores Stik batten Scie woh ee

The generalized section given above for the Potsdam series, below the Mendota
- base, holds true for a large part of the central Wisconsin district, and would be sat, 4

isfactory for all of it but for the facts next to be stated. 4 . —

+. Prof. Irving then proceeds to describe layers of sandstone and bowl.
to conglomerate occurring near the pre-Cambrian quartzite, which

_ . apparently occupy a higher position and extend downward across the
ie) upper portion of the eastern Madison section. He explains this occur-
rence on the theory of the accumulation of these conglomerates and
sandstones near the shore line at a higher level than the sandstones
that accumulated offshore.

The beds of passage between the Potsdam and. Lower Magnesian series include, a 4

already said, two well marked beds, 60 to 90 feet in ‘combi’ fitigkunes ane Men-
dota limestone and the Madison sandstone.® he.

Of the fauna in the rocks he says: .

To the list of fossils of the lower sandstone series given by Prof. Hall but little has
been added by the present survey, as far as central Wisconsin is concerned. * 2

- The general grouping of upper, middle, and lower species appears to hold true as
regards the order, but his lower species must really be assigned to the middle of the

series, since its thickness is about twice as great as Mr. Hall supposed. - : _ E

ro

1 Op. cit., pp. 261, 262. 3 a
2The Lower Silurian rocks. (Geology of central Wisconsin.) Geology of Wisconsin, survey of i

ar 1873-1879, vol, 2, 1877, p. 529. - pes a
3Qp. cit., p. 534. 4 Op. cit., p. 536. 5 Op. cit., p. 542. °Op. cit., p. 545. Y &
aN

eter NT ee ng hare es
- Hy - eo in! Rieke: aera thd BES a 4 ¥ wo n~ ko ' < ? oe ”
i * ye aie: k hes rz %
ss; | SUMMARY —UPPER MISSISSIPPI VALLEY. 2 Ooo
=a

“the: ‘Mississippi ‘Valley, in Southwestern Wisconsin, Mr. Moses
mg estimated the total thickness of the Potsdam at 800 to 1,000 feet,
th inequalities in the surface of the underlying Archean rocks being
the , principal source of its variation.! The formation is composei al-
m ost entirely of sandstone. The only exception to this is the stratum

: te strata of the formation are usually composed of fine siliceous sand, generally
small, rounded, water-worn grains of almost every color, the most frequent being
the various shades of yellow and red, sometimes green, and often snow white. The
t trata vary greatly in consistency, and in different TES the same stratum may
present different degrees of hardness. Some of the layers, and especially the white
ones, are frequently almost as compact as quartzite, and from this all degrees are
found, to a loose, friable sand that crumblesin the hand. * * * Thestratification
‘the Potsdam is very regular and even, and the beds usually lie in a nearly hori-
Z zontal position over large tracts of country, Indeed, so little do they deviate from

n apparent level that the dip can not be distinguished by the eye, but only by a
: Serefat measurement. The dip is usually to the northwest, and seldom exceeds 8 or
10 feet to the mile, but more frequently it is less.?

The most highly fossiliferous portion of the formation occurs in west-
rn Wisconsin. The formation is divided in the lower St. Croix dis-
trict, by Mr. L. C. Wooster, into four horizons, as follows: (1) “Kau
Olaire grit; (2) Eau Claire trilobite beds; (3) Hudson trilobite beds,
and (4) line of junction with the Lower Magnesian limestone.” In this
| region it borders upon the metamorphic.and igneous rocks to the north
and east, and touches the Lower Magnesian limestone on the south and
“west. . BE ni

: pe horizons mentioned are described as follows:

The Eau Claire grit, exposed at the mouth of Eau Claire River, is a very coarse sand-
‘stone, with Scolithus tubes in one or two of the layers. The rock is so coarse that it
; has been termed a conglomerate, not without reason.

The Eau Claire trilobite beds are characterized by several species of trilobites not
id found at any other horizon, and also by being the lower limit at which brachiopods

r eons matter in the formation.

_ The Hudson trilobite beds lie at the best defined horizon in the sandstone. These
‘beds lie in close relationship to and between the Lower Calcareous band and the layers
hy vhich are richest in green sand, and thus can not well be mistaken. * * * The
shaly layers below the trilobite beds are intensely green from the presence of green
a (a variety of glauconite), which, so far as known, is true of no other horizon.
The line of junction with the Lower Magnesian limestone may, in nearly every instance,
berecognized by the heavy brecciated beds of limestone just above. But this char-
acter may fail in the extreme southeastern border of the district, where it is possible
‘that beds of sandstone are interstratified with the lower layers of the Lower Magne-
‘sian limestone, as in eastern Wisconsin.+

-1Geological formations. (Geology of the Mississippiregions north of the Wisconsin River.) Geol-
io gy of Wisconsin, survey of 1873-1879, vol. 4, 1882, p. 45.

2 Op. cit., pp. 39, 40.

Sa 8 Detailed geology: [Geology of the lower St. Crox district. ] Geology of Wisconsin, survey of 1873-
+1879, vo. 4 1882, p.109. —

Op. cit., p. 110.

Ss on E

a > =. p, ‘

were found in the sandstone. These beds likewise mark the lower limit of calea-

a

= 23 siete samt eae ae horizon of ee Mendota limestone aa :
~ tral Wisconsin. |

‘

1 ks no one point in the district is the entire formation exposed, and 20, a ) obta in
the entire thickness from the Lower Magnesian limestone to the granite below, the )
ane sum ef the thicknesses of the subdivisions is taken: : Kime -

ok -
ca oad i: Feet. Z
Sa From the Lower Magnesian to the Hudson trilobite bed....... 200 ©
3% From the Hudson trilobite bed to the Eau Claire Trilobite bed. 200 -
age From the Eau Claire Trilobite bed to the Eau Claire grit...... 240. =.
he From the Eau Claire grit to the erent (at Eau Claire), esti-
ope mated ..---...-.-.---. ac ga cubs sma a ds we aheth et rasmaen 6 aaee 100

2 Toll. coe. 20) oes eoedodas caro Salen reteset 740 =

>

ae The last division is mene much thicker to the south and west, =e the 6
thickness of the formation range to 800 and 1,000 feet. ty

The report of Prof. Wooster contains details of numerous local see-
tions that show the lithologic and paleontologic characters of the Fon m ae
tion. 3 =

The outcrops in Iowa are the continuation of those of southwestern

' Wisconsin; and very little is added to the knowledge of the nat a
in Minnesota, where it is called the St. Croix sandstone by Prof. N. 1

Winchell. At Winona and Stockton there are about 303 feet of t
- formation exposed? ;

A generalized section in Minnesota, as given by Prof. Winchell 3 ig ‘is

as follows:

=

i
be

Feet.
Jordan sandstone...........-.<« .---. 75-100 = Madison of Wisconsin.
St. Croix? St. Lawrence limestone........---- 0- 30 = Mendota of Wisconsin. _
Dresbach sandstone and shales.... 200. 73
Shales 2s... 552-5 5--65. bw oN Ou og be scieles pe we me (3

z= . CANADIAN EXTENSION,

In the account of a deep boring at Rosenfeld Station, on the Canadis
Pacific Railway, Dr. G. M. Dawson corr elates the upper portion of tl
section with the Maquoketa shales, beneath which occurs the Galena
limestone, passing below into Trenton and then to the St. Peters sa ni l-
stone. Below this, before reaching the granite, there are 110 feet 0 of
dark red, reddish and greenish, bluish and grayish shales, passing / ee

. sian limestone.‘ Whether the St. Croix sandstone is represented in
this section can not be determined in the absence of paleontologic evi-
— dence, but it is not improbable that the horizon of the St. Croix and: the
Lower Magnesian limestone of the Minnesota section may both be in-
cluded between the limestone and the granite at the bottom of the babe ll.

= - =
ry R i a +See

1Op. cit., p. 112. 5
rab 2The Geology of Minnesota, vol. 1 of the final report. 1884, p. 258. “Sy a
‘ $ Winchell, N. H.: 14th Ann. Rep. Minn. Geol. and Nat. Hist. Survey, 1886, pp. 325-337. .
4On certain borings in Manitoba and the Northwest Territory. ira Soc. elles roe and Tr ans.»

vol. 4, section 4, 1887, p. 86.

a | SUMMARY —PAKE ‘SUPERIOR SANDSTONE. 7 BOO :

a 3

Sena as LAKE SUPERIOR SANDSTONE. |

‘The Sacticr geologists speak of the Keweenawan series and the hori
zontal Lake Superior sandstones as forming part of the same terrane,
and this view has been sustained by some more recent writers. Many
0 thers, however, have held the view that the horizontal sandstones
were the equivalents of the fossiliferous sandstones beneath the Mag-
: “nesian limestone of central Wisconsin, and that the sandstones of the
‘EK Ceweenawan series were nieonteviiabty subjacent to the horizontal
"8 andstones. Prof. Rk. D. Irving, taking the latter view, says:

The constant horizontality of the sandstone series, its restriction to low levels,
t the actual unconformity visible in Douglas County, the proximity of the horizontal
‘Ba Kdastonce to the enormously thick perpendicular fragmental beds of the Montreal
River, and the relations of the two series on the St. Louis appear to amount to dem-
F onstration. In the Thunder Bay region the Canada geologists have proved a similar
x Bewetornity, and Sir William Loaut's arguments would seem to show that the
same is true for the southeastern shore of the lake. That it may at times be difficult -
to tell whether we have to do with the Keweenawan or the newer sandstones is un-

- doubtedly true in some of those cases where the Keweenawan beds have a low incli-
a D ation, but such cases of difficulty are rare.!

P Wisconsin pre-Cambrian area and the fossiliferous sandstone on the
_ southern side he says :?—

~ to which the Lake Superior sandstone has been seen reaching, it appears improbable
_ that any connection ever existed between the two formations in the Wisconsin-Min-
Z proces tegion- * * * It appears, on the whole, that the evidence is all in favor of
an approximate equivalency of the Lake Superior and Mississippi Valley Potsdam
_ sandstones. It seems probable to me, with my present knowledge of the facts, that

- lithological peculiarities are to be explained by corresponding differences in the an-
= _ cient rocks from whose ruins they are built.

‘Under the designations of the ‘‘ Kastern sandstone” and “ Western
- sandstone ” Prof. Irving -describes the horizontal sandstones of the
- south shore of Lake Superior. By the “ Eastern sandstone” he means
2 sandstone that fills the valley between the Keweenaw or main trap
. _ range of Michigan and the so-called south range. The eastern end of
_ this depression is occupied by the waters of Keweenaw Bay. The sand-
a _ stones skirt the shores in a band varying in breadth from a few rods to
1 or 2 miles, the older crystalline rocks occasionally reaching down
to the lake. These conditions prevail as far eastward as Marquette,
a beyond which point to the eastward sandstone forms all of the shore
- olifis as far as the Sault. : :

1 Geological Structure of Nostiain Wisconsin. General geology of the Lake Superior Region
- Geology of Wis., Survey of 1873-79, vol. 3, 1880, p. 23.

4 -2Op. cit., pp. 24, 25.

_ *The Copper-bearing Rocks of Lake Superior, U.S, Geol. Surv., Monograph, vol. 5, 1883, p. 351.

~ Of the relation of the horizontal sandstones on thie north side of the :

Ps: An absolute proof of their exact relations is wanting, because nowhere as yet have _
_ the two been traced into each other. Judging from the low altitude above the lake —

3 they were deposited in always disconnected basins, and that their sharply contrasted -

Se SOARES gS MSG aes ps pa ap be
heres he ty im SA Aw Be. gs BMS, rat oe a
% ; Pie is 5 ne hip ie GC Ree
earn eae ‘THE CAMBRIAN. aye sae Bea
ee z “3 =. Ae: =e ese
Big Ane AEE ES of the sandstone and. its relation to — su se oy race

— rock are stated as follows: - ct PN

Thesandstones of the Keweenaw Bay and tia v vi vicinity, and eastward thence to White
_ Fish River, are reddish and often highly argillaceous. At White Fish River the red
sandstone is overlain by a light- colored sandstone, which is in turn succeeded by a
magnesian limestone, in which are casts of Pleurotomaria. This limestone is the p
Lower Magnesian of the Wisconsin reports and the Calciferous sandrock of the East- - :4
ern States. That it is succeeded in regular order by the fossiliferous limestones of
the Trenton, Cincinnati, and Niagara groups was long since shown, and has been
demonstrated anew of late years by the labors of the geological surveyors of Wisconsin a
aud Michigan. There thus seems little room for doubt as to the correctness of the :
view held for years by a succession of geological workers in the Lake Superior region E
from Owen to Rominger, viz, that in the Eastern sandstone we have to do with the

; same formation, or with its downward continuation, as the fossiliferous Cambria D
sandstone which, in the Mississippi Valley, forms the base of the Paleozoic column, : Lo
. The Western sandstones, or those of the Apostle Islands and the ad.
i joining coast of Bayfield, Douglas, and Pine Counties, are composed of
a horizontally placed sandstone, closely resembling in character the
' Hastern sandstone of Keweenaw Point. The exposures of the sani
stone are almost entirely restricted to the vicinity of the shores of the |
lake, on the mainland, and the Apostle Islands, and have never been
seen reaching more lant 50 feet above the lake level. Farther west, <
however, in Douglas County, the horizontal sandstone reaches to 360
: feet above the lake.2 Prof. Irving states that. the prevailing color of
this rock is some shade of red, from bright brick red toa brownish
red or purplish red. Pinkish, straw-colored, and even nearly pure.

_ white varieties occur, either blotching the ordinary red rock in small
patches, or occurring in layers from an inch to 2 or 3 feet in thicknes =
A section typical of many of the cliff exposures of the BES shore isas

4

follows :
Ft. In
Red marly clay (Quaternary) .sewod ss. coue.s ed wesccccun eens aed
Shaly sandstone, in layers from one-fourth to one-half inch thick ;
light reddish to brown, apse Eee, chiefly made up of
subangular quartz grains. ..........-.-- Sick phgititalels Satta 4 9
- Compact-sandstone:.2.52.4 5 saseh eens ten eee abe ssaves ais Sadoeeee 2 0
< Shaly sandstone ........... @ tee nee cece tenes ce neee boise cube est 0 3

Compact sandstone ; pinkish and moderately coarse-grained,

: chiefly made up of quartz grains, but many white clay spots,
ie eee indicating the decomposed feldspar. ......-.. a ice teeteeernas SaeeD
14 0 |
The shaly and massive layers are, however, not constant, and either will grade ,
into the other in a short distance, the shaly kinds being often merely a result of
weathering. Often the massive layers have a thickness of 5 feet and upwards, an 1

lie together in considerable thicknesses without intervening thin-laminated seams,

In many places round bunches of red clay, from an inch to several feet in diameter, ar ys
seen imbedded in the massive sandstone. In other cases the clay lies in limited a
So ————
_1Op. cit., pp. 251, 352. et ee
_ 2The Lake Superior Sandstone. |Geology of the Eastern Lake Superior District.]. Geol. Wisco: aD :
sin, vol. 3, 1880, p. 207. t , =

°! Sone
ae

0 LS i ee eee em iM donc eee a i Sgieck & tocahs nay tt ye aL Oe
ean ee aCe es Rea ys Mae ee ae
waucorr] _ SUMMARY—LAKE | SUPERIOR SANDSTONE. 337
. pe ae ' pe VASE 3 si *

the eines seams, Kos a fraction of an Sion to ot ckal inches thick. Some of the
Rw ane clay patches appear as if formed by the decomposition of granite or gneiss
_ bowlders imbedded i in the sandstone at the time of its formation.!

In speaking of these same sandstones Mr. E. T. Sweet says:

38 regard to the age of the Lake Superior sandstones, but very little in deed can be
Se roarioa in the western Lake Superior district. So far as my observations have ex-_
- tended, the sandstones are absolutely devoid of organic remains. They are removed
many miles and are separated by intervening older formations from the unmistak-
haa Lower Silurian strata.

He considers it has been conclusively shown ev the sandstones are
7 = more recent age than the Keweenawan strata

sandstone. that its Lower Silurian age was unequivocally proved by its
i stratigraphic position. In its whole extent it is visibly overlaid by cal-
4 _ careous ledges containing fossils peculiar to the Calciferous formation,
OT, in other cases, by the Trenton limestone. He describes the sand-

B inits two sections, an upper and a lower one. He says:

The upper section is composed of light-colored, almost white, sandstones of generally
soft, friable nature, The lower section is intensely red colored by iron pigment, and
ce contains varioushard, compact ledges, which are valuable building stones. West of
e Eesauetic only the lower section of the group is developed; east of it the heights

are formed by the upper division; the lower has exclusive possession of the shore as
_ faras Grand Island Bay. East of Grand Island Bay the upper division sinks down
PD to the level of the water, and only i in limited spots the lower red-colored strata come -

~ to the surface.?

On Laughing Whitefish River a section as determined by Dr. How
“ inger is as follows in ascending order:

*
%y
a
&

Ve.
-

~
No. 1.—Alternations of thin-bedded, hard, often micaceous sandstone slabs, Feet
“ with arenaceous shales (as exposed)... ... 2.6.2. 22. e oe oe cee eee 25
| No. 2. =A fine-grained, more or less argillaceous red sandstone in layers of
Z 1to 3 feet in thickness with seams of red shales ........-...-.--.- jo

es No. 3. 2k hard, coarser-grained, red, or speckled sandstone in heavy ledges up
a to 4 and 5 feet in RE AS amounting in the aggregate to 15 or 20

oS Stay i ee MS She gd NS Ae 15-20

‘ No, 4.—Light-colored, middling soft sandstone in thick layers with seams of
es _ quartz pebbles, followed by a few feet of a dark and coarse conglom-

erate; thickness not accurately ascertained .........-....-.------ 00
y No. 5.—A series of thin-bedded, soft, whitish sandstones, each layer separated

We ‘

‘ from the other by.a narrow seam of bluish shale.........--....-.. 75-100

3s 6.—Massive soft white sandrock, projecting in vertical walls ........<. 5 50
_ Directly above this, strata of the Calciferous sandrock occur with

_ casts of Pleurotomaria.‘

- This section of Dr. Romin ger’s is not altogether complete, but it shows

~ conclusively that the Lake Superior sandstone in the vicinity of Mar-

a} Lake Superior sandstone [Geology of the Western Lake Superior district]. Geology of Wisconsin,
_ Survey of 1873-’79, vol. 3, 1880, pp. 208, 209.

. 2Op. cit., pp. 351, 352.

and # Paleozoic Rocks. Geol. Survey Michigan, Upper Peninsula, 1869-1873, vol. 1, pt, 3, 1873, pp. 80-82,
Ma ae »PP. 88-90, ,

: Dy es :

Bull. 81—22 : 3

Dr. C. Rominger concluded from his studies of the Lake Superior |

- stone east of the Copper Range of the Keweenaw Point and divides it .

Pe

“

Re ee ee ey eke Ee Bid ee Seen aes £
“ 2! 5 a ae 2: % ‘ee F :

x < 7 P-4° oa . ety a = ow x : sia < > * ; * = 3E =

+ 2 Mi S-= a4 3 rewne "eens ? ene ae

or he. ” ~* io ‘. = pal 4 5 x ——* wt ae ~ = 4 a
~ : s PES as Sree er
338 . THE “CAMBRIAN. if =f Ae

a. ‘i > oe. = *

eS YT

_jon. The Potsdam sandstone is habitually horizontal, while the Keweenawan i

lent to saying that the horizontal sandstones were not then in existence. The obser-—

Fedolie. or east of Marquette, occupies the exact sixatiaraphts position D Of y
the fossiliferous St. Croix or “ Potsdam ” sandstone of Wisconsin. The
description of the character and geologic equivalency of the sandstones |
of the south shore of Lake Superior as given by Prof. Chamberlin ac-
_ cords with the view I had formed from the study of the literature per-
taining to the subject. Although not considering it proved that the two.
sandstones are exactly contemporaneous, I think that for all practical -

co

geological classification they may be considered equivalent deposits.
This view is so well caper by Prof. Chamberlin that as is. here oe
quoted: : a

Lake Superior sandstone.—-The sandstones on the southern side of the Abotison Isl- |
and are light-colored, being mainly yellow or white, varying locally to pink, brown,
and green. They are nowhere bodily dark. An easy explanation of this is found in
the fact that they were derived from the light-colored quartzose and granitic rocks —
of the southern face of the land. But passing around to the Lake Superior Basin on
the northern side of the island, where erosion preyed upon the iron-bearing nomi ee
of the Huronian series, and more especially upon the traps, sandstones, and shales 01 !
the copper-bearing series, the resulting beds are not only reddish brown in color, but |
contain a notable ingredient of iron and of shaly material derived from those forma-—
‘tions. Indeed the deposit bears a very close external resemblance to the sandstones
of the Keweenawan series, and the two have been considered as identical by able-
geologists. ia

Concerning the distinctness of the two formations we entertain no doubtful’ opine

tilted, indicating that the latter partook of a general stratigrapical movement which’
did not affect the former, which, considering the attendant circumstances, is equiva- ae

vations of Mr. Sweet in Douglas County are further proof of this.! The Potsdam _
sandstone there. abuts unconformably against the Keweenawan traps and contains
pebbles derived from them, showing not only that they were earlier formed but that
they were tilted and extensively eroded at the time the horizontal sandstones were "
formed. The local disturbance of the latter doesnot vitiate the force of the evidence —
when critically considered. Similar phenomena are presented along the sopithecnans rm
face of the promontory of Keweenaw Point.? — s
Besides these stratigraphical evidences of distinctness, the microscopical observa.
tions of Prof. Irving and the chemical analyses of Mr. Sweet show an important cones a
stitutional distinction between them. Whereas the Keweenawan wungevense are
largely nonquartzose, the horizontal beds are hi ghly quartziferous. a7
As the latter are traced eastward along the south shore of Lake Superior they are.
found, according to Dr. Rominger, to be interstratified with and graduated into the
light-colored sandstones which prevail in the eastern portion of the upper peninsul
of Michigan, and which are traceable into direct continuity with the light-colore
sandstones of Wisconsin. The same geologist (as also Foster and Whitney) is author.
ity for the statement that in the Keweenaw Valley Silurian limestone overtion this 7
sandstone. ~*t-
The southern light-colored sande like their northern equivalents, abut u 1

op

-1Geol. Surv. Wis., vol. 3, pp. 340-347; also 350-352. | ae

? This has recently been denied by Dr. M. E. Wadsworth, but more recent examination by expel ri
enced observers shows his discussion of the subject to be more pronunciative than trustworthy. Bul.
letin of the Museum of Comparative Zoology, at Harvard College, Geol. Series, vol.1. The be in
detail as determined by the later observations will be found i in Prof, Irving’s eaters Toperta 01
the copper-bearing series. a

~

-*Geol, Wis., vol. 3, pp. 15 and 350, and microscopical Pl, x1x 4. ee ae Ss

ees

red Potsdam sandstone containing characteristic fossils reposes unconformably
and against Keweenawan cliffs and occupies depressions and valleys formed
ugh its erosion. Conglomerates derived from it mark the junction of the two

Keweenawan rock for one side and Potsdam sandstone containing shells of Lingulepis
maformis for the other. The phenomena absolutely forbid any explanation based
fe faulting or intrusion

- North of St. Croix Falls the same strata, sustaining a like stratigraphical relation-
‘ sh \ip (thongh 1 not seen in actual unconformable contact) may be traced more than half
Way across the Keweenawan series, Passing the remainder of the interval to Lake
Superior the horizontal red sandstones are found abutting, in similar unconformable
contact, against the eroded Keweenawan series as above stated. The accompanying
se tion illustrates the general relationship, but only a careful study of the details
. can make clear the full force of the evidence,
| _ When to these considerations there are added others less susceptible of brief state-
m ent, to which we are here confined, it'appears that the distinctness of the horizontal

its reference to the Potsdam series is sustained by a weight of evidence that would not
Fhe e seriously questioned but for complications with what we deem the misinterpreta-
‘ tions of other geological features of the Lake Superior region. The modifications

ay which the formation assumes in that region are precisely those which its method of
de erivation demands.'
CANADIAN EXTENSION.

rn the geological map of the Dominion of Canada, published in
“1882, the Nepigon series of rocks is colored Cambrian, both on the
“shores of Lake Superior and about Lake Nepigon. This is in accord-
a ance with the views of Dr. A. R. C. Selwyn.

* ae
Be :
The Cambrian rocks in Missouri occur in the southwestern portion of
Es ‘the State, about the Ozark Uplift. As far as known they are of Upper
¢ Jambrian age and consist of a sandstone that occurs beneath the third
_ magnesian limestone, or Calciferous, and the fourth. maguaesian lime-
stone of the Missouri survey, beneath which, according to Prof. G. C.
Broadhead, there are other arenaceous and calcareous beds. .
Yhe third sandstone is doubtfully identified by Mr. I’. B. Meek, in
Y iller County, as 6 feet of white sandstone, composed of rounded grains
of quartz cemented in part by calcareous matter. Subjacent to this
ot Ethrore are 27 feet of hard gray and light flesh-colored magnesian lime-
‘stones in rugged, irregular beds from 5 to 8 feet in thickness. In
Morgan County the third sandstone is known to occur at a few locali-
| ? ties, where it varies from 25 to 30 feet in thickness. The subjacent fourth
1 magnesian limestone forms a bluff 150 feet high above the Osage River
‘in the southwestern part of the county.’

“Si

MISSOURI.

-

- 1General geology. Historical geology. Paleozoic era. Geology of Wisconsin, survey of 1873-1879,
_ vol. 1, 1883, pp. 122-124.

_ # Reports on the Geological Survey of tho State of Missouri, 1855-1871, 1873, p. 127,

% 1p, ae ee 148,

“ basta ‘apainet Stoded elif of oweuhwan rock. At St. Croix Falls light- —

ations and contain Potsdam fossils. Hand specimens may be obtained, having ©

‘Lake Superior sandstone from that of the Keweenawan system and the correctness of

se aeal BT ates ete, ee ee hap ee Ye Mee eS are ae
See ¢ re ee oe gt. ee ee, Fe

Me
> ih
> "

-

—

eat sae oa oe a THE | CAMBRIAN. ah A reac RE

Francois. The entire thickness of this as well as the regular order of its various | <

: : diamond -drill on the Mine La Motte property indicate magnesian limestone, bio somal .

-

~ beds and sandstones rest unal bere on the porphyry, and on Big Creek, Iron County, —

| i Fane’. The order of deposition, commencing at the oldest, is—

ae 5 , .
x ae tyy ey aes a oy? 5 4 pe oe or os art Mate aa < r
te TAP Ee tet LOX. a ; =e CS is 5 Ree y ee
yn She * Se aet Bee | ges Gene ; Oe 5 tS . TT a on pant = Jyh
* a aes oa =e ee oe, te = 4 2

sot

In Madison, St. Francois, and Tron Goniticn, Prof. G. Cc. Broathent
found beneath the third magnesian limestone the following downvard i
succession : eer

(3) Siliceous or grit- stone bed, with mitoeenaden. magnesian lime- é

_ stone. : . Bi
(2) Marble beds. | . Bt ak zy 3
(1) Sandstones, conglomerates, and shales. 4g a

In No. 3 Lingulella lamborni Meek has been found. The marhil a
beds or No. 2 appear to be confined to the southwest quarter of Madison. 7
and the central and northern parts of Iron and extend into Reynolds —
County. The greatest thickness is not. over 30 feet, and they are nope
always present. . Se Sey,

(Ose
‘ =

No. 1 is confined chiefly to the northern part_of Iron and Madison, extending to St. |

beds is rather difficult to arrive at. But we find both in Iron and Madison Counties —
coarse conglomerates resting on granite and porphyry. We also find sandstones, —
which are sometimes very coarse, and at other times fine-grained, resting on con- —
glomerates. We also find shale or slate beds reposing on granite and underlying sand-
stone. Similar shale beds are also intercalated with the sandstone. In the neigh- ~
borhood of Mine La Motte this sandstone reaches to over 100 feet in thickness, and |
is also found to be the lowest rock. directly resting on the granite, Borings wit a

siliceous beds, 80 feet; sandstone, 63 feet; granite. |
On St. Francois Pivee in Madison County, these lower sandstones rest directly on —
the granite and are unaltered; on Twelve-Mile Creek, Madison County, the marble —

heavy beds of unaltered magnesian limestone rest directly on the porphyry.) wa ne

At the deep well of the St. Louis County insane asylum, beneath the
third magnesian limestone, the drill passed through, going down— __ 4q
98 feet of third sandstone. ,
384 feet of fourth magnesian limestone.
54 feet of Potsdam sandstone. ,

_ At the base of the sandstone it entered what was supposed to De
granite, although the line of demarkation between the sandstone ane ye
the granite was not well defined.? - s
_ In the descriptive geology of Madison County Prof. Neoarheus stat es ;
that the sedimentary rocks were deposited across the valleys between.
the mountains and the hills (that is, of the old pre-Cambrian land su

(1) Sandstones, conglomerates, and shales. “oF

(2) Marble beds. ; —

(3) Grit-stone beds and rough nee of magnesian limestone. za *
Above this comes the magnesian limestone referred to the Calcifero US.
In the vicinity of Fredericktown there is a series of grits between the
grit-stone beds and the superjacent magnesian are in which a -

1 Geological Survey Missouri, including field work of 1873-1874, vol. 1, 1874, PP. 31, 32.”
Op. cit., p. 32 ;

.

"of the ‘magnesian limestone Lingula lamborni, Payee a fienamiod

_ observed. He states that probably this magnesian limestone can also
be included in the Potsdam zone.’ This includes all the limestones 1 up
to the base of the recognized third magnesian limestone.

We more detailed account of this lower marble belt is given by the
% “same writer in a description of the marbles of southeastern Missouri.
~The most typical section is that of the northern part of Madison County,
4 which is summed up as follows:

, age ¢ 8 Magnesian limestone. .

(2) Eighteen feet of thick beds of siliceous dolomite and thin shaly limestone,
. with Lingula lamborni.

g (3) Twenty-three feet of gritty abtomite:

=. (4) Five to thirty feet of marble.

(5) Five to forty feet (as much as 90 feet near Mine La Motte) of sandstone.
(6) A few feet of slaty sandstone resting on granite.

_ assign the marble beds to the Potsdam group.?

a 7
_ EASTERN BORDER OR ADIRONDACK SUB. PROVINCE AND ITS CANADIAN EXTEN-™
SION.

Z The geographic distribution of the Potsdam terrane about the Adi-
‘rondacks is delineated on the geologicai map of New York accompany-
ing the final report in 1842, and that of the Canadian extension on the
‘small map accompanying the 1863 report of Sir W. E. Logan and the
pares map of Messrs. Logan and Hall, published in 1866.3

_ On the western side of the Adirondacks the outcropping of the sand-
stone is first seen in the northern part of Lewis County, where it rests
_unconformably upon the subjacent Archean rocks and passes above

4 broadens to the north in Jefferson and St. Lawrence Counties and
| extends around the northern side of the Adirondack area through
s ‘ranklin and Clinton Counties to Lake Champlain. The exposures on
f the eastern side are more or less interrupted, and rarely occur upon the
- eastern side of the lake in Vermont, except in Addison and Rutland
Counties. On the southwestern side outcrops occur in Washington,
4 Warren, and Saratoga Counties.

~ The Franklin and Clinton County area extends across the homndaiy
into Canada, forming quite an extended exposure within the triangle
formed by the St. Lawrence and the St. John’s Rivers and the bound-
ary, and at one point it crosses to the north of the St. Lawrence River.
‘rom St. Lawrence County the sandstone crosses the river and extends
Bae the western side of the Ottawa Basin.

_ 1 Geological Survey Missouri, including field work of 1873-1874, vol. 1, 1874, pp. 357, 358.

_ 2Marble of Southeast Missouri. Kansas City Review, vol. 5, 1882, pp. 525, 526. -

_ Geological map of Canada and part of the United States from Hudson’s Bay to Virginia and from
ul Missouri River to Newfoundland. Montreal, 1866.

341

4 The presence of Lingtla lamborni in beds a little above the marble will certainly |

pr yasteropod, and a coral, resembling in cross-section a Zaplirentis, were ©

/

‘into the calcareous layers of the Calciferous formation. The outcrop

river has worn a caiion through these beds for three-quarters of a mile |

Rees

< . ~~ o = 5 < an met ; tame fy eS

aa ee ale ae ate tt iad 2 tS SL ke ee eee Bhat Sec vig te
3 HON. . “< eat se Pid Dee
3 Be Ne _ THE “CAMBRIAN.. eas oa

in St. Lawrence County, there are but 60 or 70 feet of the rock exposed,

’ stone in massive layers. At the Narrows, three-fourths of a mile fe

. - 4 " to => — ¢ eo
_* — zr ~ —

Gutecavas Chasm, in Franitin Oonnes Au Sable Chios, + in Es ek
County, and Greenfield, in Saratoga oem? in the State of Ap ew York,
and Hemmingford, in Canada. ~ ee

Section at Potsdam.—At the type inane of the terrane at Potsdam, 4

~It occurs in layers from an inch or two in thickness up to 2 feet, and.
the general color of the mass is yellowish brown to reddish chic par. 7
ticularly the latter color in the thicker layers.

Section at Chateaugay Chasm.— At. Chateaugay Gide Franklin
County, one of the best sections of the formation upon the northern
slopes of the Adirondacks is exposed. I studied it in 1888 and found
that 5 miles south of the Ogdensburg and Lake Champlain Halla
the pre-Cambrian rocks are to be seen on the hills west of the river a
in a few small outerops about one- half a mile to the north. It isa
bedded, reddish gneissoid and hornblendic rock, probably of Algonkian
age. Nearly one mile south of these outcrops the. Potsdam sandstone 5
appears in the bed of the river, with a northwest dip of about 3°. The
exposures increase rapidly in thickness, and bluffs from 50 to 75 feet
in height, formed of evenly-bedded layers, rise above the water. The

down to a mill and pond, where the cliffs break away, and the strata,
losing their dip, continue to the south, in nearly horizontal seer to the
crossing of the railroad embankment. a

The fall in the river bed is rapid, and at the High Falls of the Cha a
teaugay Chasm a bluff of 125 feet rises from the foot of the fall. | ‘The
lower 35 feet of the section is formed of coarse reddish and gray oa z

ther down the stream, the lower beds are 75 feet in thickness and pass
into massive bedded grayish and buff-colored sandstones that break up,
into thinner layers on exposure to the action of the weather. Many | of
the massive beds are made up of irregular cross-bedded layers: this i
best seen about a mile below the falls. The strata below assume asoutl
westerly dip of 2°to3°, which carries the entire sandstone formation be
neatha hard light gray sandstone a little north of the mouth of the chasing n.
One hundred and fifty feet of sandstone, not included in the section Dn
above the railroad embankment, is exposed in the chasm and q >
feet of the upper beds occur below the mouth of the chasm. This gives
a total thickness of 250 feet of sandstone as the known thickness 0 f
the Chateaugay section. To this there is to be added an unknow!
amount at the base and 25 feet of passage beds between the upper sand-
stone and Calciferous sandrock, to be seen just above the entrance ¢
Marble River into the Chateaugay. ; | a s i

Ye * 6
x 4

ee Ex nfs As SECTION.
(From the base upward.)

= 1) Coarse Masiotorie with occasional layers of conglomerate near the base...... 75
F: eats. “Color reddish brown near the base, buff, gray, and buff and gray, spotted
mee -- - with grains- of reddish brown sand. Texture is ads and hard, with
bands of a soft friable nature.

% | (2) Massive bedded, grayish and buff, meoher coarse sandstone, many of the ae

IIIIITIININD G2 hoo 8S ois on bind sb canes sewn 'e ve chee ono cet suse vous 150
(3) Compact, fine-grained white sandstone, some of the layers of which are dis-
= colored and broken by small reddish brown cavities. Lingulepis acuminata

occurs in the upper portion, and 10 feet higher up ie ing compacta,

4 oueemeennarueap, 1, Piychaspie-ap.? cscens toccce coco ca sees snccessddenben 25

The stratigraphic exposures are not continuous, the section being
Pecken in places by concealment under the drift. Nos. 1 and 2 are

x = furl well connected by lithologic features and No. 3 rests on typical
_ strata of No. 2, only a short distance intervening between the outcrops.
2 No. 3 is well shown on Marble River one mile southeast of the Cha-
- teaugay Chasm, and the Calciferous sandrock is shown a little farther
~ down the stream. The Species found in the upper part of No. 3 are
_ jdentical with those found in the limestones of the Upper Cambrian in
Bpartoga. County, New York and fully prove that the fauna of the

_ Potsdam sandstone is the same as that of the St. Croix sandstones of
Beviseonain: :
Section in Hemmingford.—To the northeast of Chateaugay, across

5 __ the boundary, in Hemmingford, Canada, a section of the sandstone
. E socnrding to Sir W. E. Logan, is 540 feet in thickness. On the south
side of: Hemmingford Mountain about 180 feet of a coarse gray
gandstone are visible, in some parts constituting a conglomerate, with
rounded pebbles of white quartz, varying in diameter from an eighth
z to three-quarters of an inch, while in some parts of the rock there are
- thinly disseminated flat pieces of black or green shale 1 or 2 inches
in diameter by an eighth of an inch thick. The general color of the
_ rock is gray, but greenish and reddish beds occur, and the three eol-
ors sometimes follow one another in thin stripes with various alterna-
tions. Above the strata of the ravine the hill contains about 120 feet
of gray sandstone, the lower half of which is rather coarse grained, and

4
i

below the same strata 240 feet. Neither the base nor the summit of
the sandstone was observed.! Farther to the north along the shore of
the St. Lawrence oceur the celebrated fossil track localities described
by Logan. ;

Section at Keeseville and in Au Sable Chasm.—About one-quarter of a
~ mile above the village of Keeseville, on the Au Sable River, a rounded
: boss of granite shows on the south bank. Nearly 400 feet lower down
the stream, on the opposite side, an evenly bedded and cross-bedded

=
H
<i

* : Geological vg of Canada: Report of Progress from its commencement to 1863. Montreal, 1863,
- 88.

sar

L

"y -
=

Ay

_ where the beds are horizontal, above the entrance to the Chasm, the

“

. New York, that serves to correlate the sections of Chateaugay and

Ne BERS ENE Bae Fo Oe Ment Qe ae Eye Cy Vel ed ee ene a ee a
SS cig. Aer, rar: PD Sit 4 Oe aes eo aie KY. ie m
Bak ri \ } y c pe 7 pte ; ma 5 4% r e
i ° D | pale or) iF ee, : ‘ ‘Sel FS J
) ew “e ene oe OY Se : eos oe
-OA4 >. Sy oye ee CAMDRIAN. Save tach aha aroun - too

_. the highest beds-observed. oon

(2) Massive layers, light gray, fine-grained sandstone, very hard, breaking up

33) Thinner bedded gray and buff sandstone, with Protichnites tracks above the

r . "2 al “= $
- s

~ compact gray sandstone occurs, lying in Seat horizontal beds. towel Ps
_down they dip 3° to 5° to the northeast. This dip increases to 70: to
8° at the iron bridge. Following across the strike down the stream to”

measured section shows 333 feet in thickness from near "the granite to

The section as measured from the mouth of the Au Sable Chasm to :
the summit beds above the fault is as follows:

‘

SECTION.

(1) Compact, fine-grained, steel-gray, buff, and light gray sandstone, in layers — m
from 6 inches to 5 feet in thickness (20 layers)........--.. PRO Pee eo ee - 45.%
Strike N. 30° E. Dip. 5° E, a

into'thin layers, 4 to-3 incheg thick... - ...<. 0.2 ss. cc. bende ncaa ceegwebe 6. .

(3) Compact, gray sandstone in three layers; 1 foot 5 inches, 1 foot Ginches,2
feet DT Avie 65s Sagcrt. oe Peed. Seppe ewes cache eee Eee ina ap.
(4) Light gray and buff sandstone, three layers. ......--.... --eces-- ene ese nne 46

) Light gray compact sandstone, with Lingulepis acuminata, Conrad sé fn baka 1
Strike N 30° E. Dip 5° E., at foot of rapids. ye

(6) Light gray, fine-grained, contest sandstone, in layers varying from 6
/ pinehes t0.18-inches:in thickness” 0.4 4. 32 secu so- Salsa gees senege med ene eae 64
(7) Of the same general character as 6, in massive layers, breaking up into thin
layers on exposure. Occasional layers contain many sinall, flat concre-
tions of clay shale and also fragments of Lingulepis. At 34 feet from
the base Hyolithes primordialis ? and Lingulepis acuminata occur near the
boat-landing in the Chasm. Thirty-five feet higher up in the same iight
gray compact sandstone L. antiqua occurs in association with Ptychoparia
WRIRUEE 3.) - = woop sane ae sade thaws s Vaneke Sémiae Veep es ramen Genk pases tee att 17,

At this line a fault breaks the section with a down-throw to the north- a
east. The river and Chasm follow the fault from the Elbow to the
Devil’s Oven, where the section is taken up again.

(1) Massive layers of light gray, hard, compact sandstone. Prof R. re Whitfield ¢ ig i
found at this horizon Pitesonbi typica, Ptychoparia minuta ......--0.-.-- 30

(2) Evenly bedded gray, buff, and yellowish sandstone, hard, compact nial in
layers 1:to 4 feet in, thicknéda /. 6 ocene de bc nado d pe coes Pobe os eee ene 165°

-mill-dam and above the bridge at Birmingham..........-....-----..----
Strike NE. ; dip 5° SE.
Ripple nigh are very numerous and Lingulepis acuminata is abundant 15 foot P
above the Protichnites bed, and extends about 25 feet to the top of the section. | {
Some of the layers are a little calcareous and full of annelid trails and borings. 2

>™ od

Estimating the amount of repetition of strata in the two sections ne
there remains a lower series of 210 feet, and an upper of 140 feet, or a) ;
total thickness ot 350 feet with the summit and base of the forrastty i Rel
unseen, a 44

— Section at Whitehall. _—There i is a fine section Scpaeit at Whitehall, |

Au Sable Chasm. At the former the upper fauna is present and at
Au Sable Chasm the Ptychoparia minuta subfauna. At Whitehall the 7

‘ a
= Vin : i
- ou SS ARG 7

ri ne Fm te goes =? ig mS Sy
) SUNMARY—ADMONDACK SUB-PROVINCE. 345

} er fauna, occurs in the upper portion of Na, 17 of the following sec-

pos ition of the same subfaunas in the Wisconsin section.
& Section beginning below lower lock of canal at Whitehall:

Ft. In
(1) Massive bedded, compact, dark steel gray sandstone, almost a quartzite. 25 0
~) Dark clay shale.-........ Wee Sade S abt ae ia thal nd mS heb oa ae ihe Bib mom aie etek 0 6
~@3) Bluish gray, brecciated limestone . gece ee eee ee cet e ee ne eee n ee eee e ee 0 6
~ (4) Fine grained, compact, steel gray nibaboné .. o searhtebineg Oaks eis aaiyh. st Nee
_ (5) Compact, arenaceous DORN es td he Dic tie, nica Se pede thie tials vss pies «a be 3 0
(6) Compact, fine grained, steel gray sandstone in layers of 6 inches to 3 feet.
3 - Partings of coarser sandstone and small, flattened clay concretions
f occur, also streaks of light-colored sandstone in the layers, and cross- ~
bedding is of common occurrence......-.---2- e202 eee ene ee ee eee e eee 14 5)
et. Annelid trails on the surface of the layers. i
Strike N. 20° E.; dip 6° to 8° E.
(7) Calciferous adiiad TIE MON ed « hep nda abn as caondebnwete Beak 2, F
x 8) Fine grained, compact, steel gray sandstone................----.---- 5.2.0
» ( 9) Thin bedded sandstone and clay shale.............--....--.--.-------- 1 3
= (10) Compact, gray and purplish, fine grained sandstone, streaked with dark
Ae sandstone and shaly matter; slightly calcareous in places -___-_.... 16 6
aly Dark gray calciferous layers, weutheriag to areddish brown sandstone.. 2 0.
_ Annelid trails and borings.
= ( 12) Gray, compact sandstone...-.. 2-2. 2. een e eee ee eee een eee eee eee ee

a3) Dark gray, calciferous layers, weathering to a reddish ar ban sandstone. 1 4.

Annelid trails and borings.
(14) Hard, compact, gray sandstone, in evenly bedded layers 6 inches to 3 feet
z in thickness of the division of the typical Potsdam sandstone. Sum-
be 3 | mit near crossing of private roadway .... 2.222... eee ween coon ne cn wene 59 8
_ (15) Sandstones similar to 14, but with few alternating calcareous layers; the
-. . ealeareous matter daediaposttig and leaving streaks of reddish and

Et EAL BET G9 IRV OTS oo oe. cocises antec bus cay beencn ca vee oes 113 0
3 _ Ripple marks occur on the surface of many layers and atinelid
bf nee trails on the calcareous strata, About 30 feet up found Paleacmea

typica, H. and W.

a Strike 25° E.; dip 10° E.
io er side The light aK compact limestone, with the little flattened concre-
ae tions of clay and the cross-bedding, give this portion of the section a

striking ponripitgnce to'that of the upper 150 feet of the Keeseville
eZ % ... Seetion, - :

(16) Lead colored calciferous sandstone, weathering rough........-......-.. 0 5
gy (17) Alternating, gray, compact, fine grained sandstone, reddish coarse sand-

~~ stone and finer calcareous sandy layers. Lingulepis acuminata and

Ptychoparia sp? occur inthe upper layers, about 40 feet up.......... 70 0
“_ + a cape ae
eS 332 5
& erie oN ; Calciferous.

— (18) Calciferous sandstone with a massive bedded light gray compact sand-
nes MUttiny V0 100Gb GHIOK «<= bv. wasee koeaec.llmcks Sosce. scale Stine pes 40
The upper 30 feet of 17 and all of 18 may be considered as the pass-
age beds to the calciferous sandstone above.

~

a) Lead colored, massive bedded, calciferous sandstone .....--......-..---- 230
(2) Lead colored, brecciated limestone overlain by a compact light gray lime-

stone ..... pee Sate aoe os ae mwas nen ce emewencs come we cscens seneee- 20

tion and the lower in the lower part of No. 15. This is the relative .

ee

“. : 1 or S 7: 1,

to = «3 45> ae oe eles -

; 4 ‘ pac = ; hee ~ « ¥- Pies o > iy Bina 5

346 a Se : THE, CAMBRIAN, jo ae : =a
ey S Sane ade

pres “Section iat PS ne section, as Acveaied. eis and west 0 vf
ar Saratoga Springs, and north as tar as Corinth, New York , has, att
_ base, about 200 feet of evenly bedded, compact, grayish to yellow us
colored sandstone, that rests cinocndeenietly against or upon spurs oF a

_ Stone, the section 3 miles north of Saratoga se gives in ascendin ng
Ewe order: i

Whitehall and at Comstock’s Landing, Washington County, New York, where it has

- closing deposit of the Cambrian; and there is but little doubt that if we could fin d
_ a fauna in the limestone (4) of the section it would serve to connect the Caphee s
-and Lower Silurian (Ordovician) faunas.! -

dam epoch closed on the south side of the Adirondacks with adeposit

- upper beds of the quartzite on Marble River in the township of Cha- 4
teaugay, and in each section the Calciferous formation is aupeoeeas to.

~ Hemmingford Mountain. Unfortunately this section has not been |

sandstones. The section at Au Sable Chasm, however, shows thata sec-

~ 1$econd contribution to the studies of the Cambrian apo of N orth 1 America, wu. set Geol. survey i

See we ee gee eae saga se
eee ee Ree oF

&

ridges of pre-Cambrian gneiss. Including the upper beds of sar a.

>. : Feet. _
(Tt) Bandatons 322> x, beens anecskareee names eect ee patch ete ies 40-
(2) Oolitic Nime@atene ic, ac soceuape ver ie wade ole See Ree Smee 30
(3) Dark gray, evenly bedded limestone........-.2.--..0eeeeeee 5O 2
(4) Unfossiliferous, impure, compact, more or less siliceous lime- __ - >.
Stone. 555% Co 0a ed Soup tns pen ae gutetna eanieeet Rae One 95

(5) Massive-bedded, slightly magnesian, gray and dove colored .
limestones with numerous small, narrow-chambered cephal- —

opods near the puntent>i 2c... ¢.<se- scmntn ueeee es sedges 35
(6) Massive layers of steel-gray, more or less arenaceous lime-

SONG 525 Go hoAse a eee ee Coe ea A te Mae Re ay ee 125
(7) Bird’s-eye limestone. .......-... peat cnet eens eens cee eee ee
(8) Black Hiver limestoné::<. so J.-40<als de cece os be auk cate eee
(9} ‘Trenton limestone ..-. ¢-navaceene weicce evans <n oe ne eee — 40

‘The limestone (2,3) capping the sandstone (1) of the section is also found at

been, as was the limestone (2,3), referred to the Calciferous. The limestone 2 and K Is 2
appears to have been,'on the southwestern side of the Adirondack Mountains, the

The following fauna was found in No. 3 of the section :

Cryptozoa proliferum. ass Billingsia saratogensis.,
Lingulepis acuminata, Matthevia variabilis.
Platyceras Tate eels: ? _ Dikelocephalus hartti.
hoyti. : _ speciosus. :
Metoptoma cornutiforme. Ptychoparia calcifera.
simplex. (A.) saratogensis.

The comparison of the Chateaugay Chasm section with that of Sara
toga County proves very clearly by the included faunas that the Pots-

of limestone carrying the Dikelocephalus fauna. It is found in- the > %

the closing epoch of the Potsdam. a si
The greatest depth reached in the formation is that of the section of —

studied so as to determine whether there is any fauna present in the

ond horizon of the Upper Cambrian a occurs about the Adiron- ‘
dacks. This is the zone of Ptychoparia minuta, corresponding | to te
zone of Ptychoparia minor of the Wisconsin section. ‘py Sse a

—

Bull. No. 30, 1886, p. 22. . C4 aaa See

-~ , - ate is ~)

a >» “
: sey See eri Valery
naa ta — 4ye~F > Pe ee ee NS

SSR ., Sue as a ee fae we, “ —_ f
a pee a ee Se sti. Pie p ans Dee i ats 2 ee oe ea
5 . ~ ‘ <

7 a ages Ra *,. ae <» »

“iw

ae canes itis DAKOTA, ie eee BAT

ce. © presence of the Potsdam terrane on the south side of the Adi-
1 ‘rondae s, along the valley of the Mohawk, has not been positively

F ably upon the pre-Paleozoic rocks and beneath the Calciferous sandrock,

has been referred to the Potsdam. The discovery by Profs. Shaler aiid
Ww illiams of a thin layer of shale, resting upon this layer of sandstone,
on the north side of the river at Little Falls, in which specimens of
_ Linguteps ‘acuminata occur, lends more authority for the statement that
the Potsdam i is present; but as the species Lingulepis acuminataranges
up into the Calciferous sandrock, both at Whitehall, New York, and
on the north side of the Adirondack Mountains in St. PROS pt aS

- it is doubtful if we can claim the presence of the Potsdam at any point
- in the Mohawk Valley. Thereis not, however, any definite reason why

beneath the Calciferous, if it is not concealed by the oyeHah 4 of the
ate Oalciferous and Trenton terranes.

The sediments of the Adirondack sub-Province and its Canadian ex-
~ tension, with a single exception, were accumulated in a shallow sea not

- far removed from the shore-line. Ripple-marked sandstones and trails

_of marine invertebrates occur. The sandstone is relatively fine-grained

_ with the exception of a small deposit of conglomerate in St. Lawrence ~

County, New York. The formation belongs to the Upper Cambrian,
and overlaps upon the sloping shores of the pre-Cambrian land. The
~ one exception to the arenaceous deposit are the limestones in Saratoga

~ County, New York, which were deposited on sandstone and overlap on

Dk
ey

that of the quartzite at Marble River, near Chateaugay Chasm, on the
- northern side of the Adirondacks.

=a “
,

tothe pre-Cambrian rocks. The fauna of the limestone is the same as

WESTERN BORDER OR ROCKY MOUNTAIN SUB-PROVINCE.

This includes the Cambrian rocks of South Dakota, southern central
Montana, central and northwestern Wyoming, and Colorado.

SOUTH DAKOTA.

_ The chief summary of our knowledge of the Cambrian rocks of the
Black Gills of Dakota is taken from the reports of Messrs. Newton and
_ Carpenter. The sandstone identified as the “ Potsdam” is the lowest
member of the fossiliferous series, and in numerous and excellent ex-
__posures its character and relations are easily determined and studied.
- It everywhere rests unconformably upon the upturned edges of the un-
<< derlying Algonkian slates and schists, filling up irregularities in their
__ surfaces, and its basal member is generally formed of coarse materials

derived from the erosion of the subjacent rocks. Consisting mainly of

| coarse and friable sandstones, with conglomerates easily eroded, it —

-__—s covers superficially very limited areas.
Bya reference to the geological map accompanying the report of Mr.
, qj Henry Newton the exposures of the “ Potsdam ” sandstone will be seen

ae 5 4 +
7 — os Bea “«
“i°? Se So L: 5 “ = ~ ot Ss
dal Sows . => : < -_

Dp roved. At Little Falls a thin layer of ‘sandstone, resting unconform-

a thin bed of it, with the typical Potsdam fauna, should not be found —

. . we ae

: (1) Argillaceous slates, dipping 60° west ..---....--.. eee cn eee oga

-reous and ina great number it contains peculiar greensand deposits. —
_ Its thickness is quite uniform, ranging generally from 200 to 250 footed

with, but one measured in the eastern cafion of Spring Creek by Mr. |

Be Se oes ra “328 Se aay tt See oe A oso Sante ly ges CB Sts Leer he SS i Manas Te
- 7 ey colt ‘. “of 4 jdexreee. » ai =f bm ona ay) ff " 2 i —* * ~ a
. Se => cee ca POR GP OE A he
ye as el tarp £3
rn} t e* 5 ree yr ak -
348 “rnn’ CAMBRIAN. Le i Sonera a
A . ;

to form a very narrow uae surrounding the “Archean” area. Though, 4
essentially a sandstone formation it has some variety of composition. —
Usually it carries a conglomerate at the base, but this is sometimes ex- |
changed for a dense quartzite, and in many places there are interstrati-
fied beds of quartzite. In a few localities the formation is quite calea- —

but attaining to 300 feet on the north branch of Redwater Creek. Com-—
plete sections from the “Archean” to the Carboniferous are rarely met

Jenney is as follows:!

_ Archean. . —

“

Potsdam.

(2) Brownish yellow conglomerate, with quartz pebbles, resting unconformably
on 1 and dippilig 25° northésats . oo. 944-00 iooc 80% be ke A eee ee 25
(3) Reddish brown sandstone, thinly bedded at base and alternating with soft, — —
shaly sandstones, containing large fucoids, Lingulepis, and fragments of. *s ;
trilobites ...... Sheet te hn Afi FLAS he ndag axieren paneer 200

Carboniferous.

(4) Reddish brown, or pinkish calcareous sandstone, thinly bedded, containing aq
~ Spirifera camerata, cyathophylloid corals, and crinoid columns.....-.. ..-- 20%

_ (5) Limestone: Spirifera camerata, Productus, etc......-..- oes bla Uhh so Sea ae 339

- identified or described by Prof. R. P. Whitfield: ?

/

_ parisons are made between it and the correlated satidhtones about the 4

Many details are given of the local phenomena presented by the sedi- —
mentation and mode of occurrence of this formation ; extended com- —

Big Horn and Wind River Mountains of Wyoming, the sandstones of

the Mississippi Valley, and the typical Potsdam sandstone about the Be:

Adirondacks of New York. a
The following is a list of the fossils found in the sandstone and i

Paleochorda prima. Lingulepis dakotensis. es
Palzxophycus occidentalis, Obolus? pectenoides. _ ae
Paleophycus. . Obolella polita. : +
Scolithus. . nana.
Lingulepis pinnaformis. Crepicephalus centralis,

cuneolus. - planus.

perattenuatus, >

Prof. F. R. Carpenter describes the ‘ Potsdam” in the Black Hills « as
follows:

The present site of the uplift existed as a slowly sinking island ini the Potsdam
ocean, probably the last surviving land of a vast area eroded and submerged by ag

Ps

1Newton, Henry: Geology. Report on the Black Hills of Dakota. U.S. Geog. and Geak ‘Survey —
of, the Rocky Mountain region, J. W. Powell in charge, 1880, p. 88, sy —
2 Op. cit., p. 107. rari Wee rie *

=

—- -sr4 ~r
—— - ay jhe
=) 3 + SJ ‘

‘the advancing waters.
a , conglomerate. The ocean advanced upon the land with an action that has been
aptly termed that of a horizontal saw. The cliffs were undermined by its action,
the débris thus formed worn to bowlders, to gravel, and to sand. As the shore-line
advanced and a given point became farther from land, it received finer and finer sedi-
a mente, until sedimentation, in this area at least, entirely ceased.!

F the central portion of the Black Hills uplift. Near Harney Peak the
last outliers are about 50 feet thick between the unconformable sub-
e Bp iseent “ Archean” rocks and the undisturbed conformable super. Jaceae
- Carboniferous limestone.

‘al

WYOMING.

_—
\

_ There has been comparatively little detailed information published
relating to the Cambrian rocks of the Big Horn Mountains. Dr. F. V.
3 - Hayden visited the range in 1861 and found the nucleus composed of
_ red feldspathic granite and a series of stratified Azvic rocks. Resting
- on these occur the sandstones which are referred to the “ Potsdam.”
4 He found a few thin layers of fine calcareous sandstone filled with fos-
sils characteristic of the period.2 These were studied by F. B. Meek,
_ who identified Conocoryphe and perhaps Dikelocephalus.*

According to Prof. T. B. Comstock, the sandstone referred to the

4

x ieee attains a thickness of about 200 feet in the region of the Wind

_ River Mountains, and above the sandstone on the eastern side, along
the central portion of the range is a series of limestones resting on the
~ sandstone, having a thickness of about 200 feet. From specimens col-
a lected in the limestone he identified a trilobite of the genus Dikelo-
cephalus, several specimens of what was supposed to be Orthis tritonia,
and a quantity of a species of Theca.* As far as Prof. Comstock’s ob-

a Sa tai

B iacent metamorphic rocks.» On the map accompanying the report the
© Potsdam ” formation is represented as occurring all along the eastern
_ side.of the Wind River range, and also along the central portivn of the
_ western side. The latter occurrence, however, is denied by Dr. A. C.
a Peale. Dr. Hayden noted in 1862 the presence of a sandstone resting

-- upon the vertical edges of the Azoic clay slate series in the Laramie

—

npr ey

y ee] oO Oo———o—onrorrmoao
; -INotes on the geology of the Black Hills. Preliminary Rep. Dakota School Mines, on the Black
. Hills of Dakota, 1888, p. 31.
_-«- 2Hayden, F. V.: Sketch of the geology of the country about the headwaters of the Missouri and
aX Yellowstone Rivers. Am. Jour. Sci., 2d ser., vol. 31, 1861, p. 234.
a Meek, F. B.: Preliminary paleontological report with remarks on the ages of the rocks, etc. U.
_§. Geol. Surv. of the Terr., Sixth Ann. Rep., 1873, p. 465.
4Geological Report. Report upon the reconnoissance of northwestern Wyowing, made in the sum:
‘mer of 1873, by William A. Jones. 1874, pp. 108-110.
a 5 Op. cit., p. 106.
Report on the geology of the Green River district. U.S,Geol, Surv, of the Terr., 11th Ann. Rep,,
1879, p. 524.
ee

spate | SUMMARY—=WYoMING. a 349 .

The base of the Potsdam dntirely around its outcrop is

He calls attention to the fact that the sandstone thins out towards —

servations extended the sandstone rested unconformably upon the sub-

ot Mountains, which he referred to the age of the Potsdam sandstone,

:

Se although no organic remains were found. In the vicinity of the hi

x ft ; wo x ~~ ‘a = Lee eis ; Dea,
Se ae ae s Matty ei fie 7 Be tes = Le Z <j ‘
Se ee is cee Re ee ag
7 ‘THE CAMBRIAN. SS OS Ra ae
itr om oe ier ee ATR =i

S= _ waters of the Niobrara River he measured a section as follows: Pp i oe

—

——

e . er
ee ca ye ’

4

~_—

“Whe

- this horizon is noted by him at numerous localities on the flanks of the

_(1) Quartzose sandstone, some parts filled with pebbles..--.....- wetn sea agkaee a
She} e200, BECILUACCONS Slate. io. nen ao op hee oes semey ee eee eee eotdenth ot Ge: sips
(3) Sandstone, dull reddish ferruginous, like bed 1 bore re ee eee = . 37 :
_ (4) A series of strata more or less inclined, dts posed of gneiss with silvery mica
in large plates, micaceous and talcose slates, white quartz, etc.

He states further that he has no doubt the Potsdam sandstone
occurs in the form of an outcropping belt all along the Laramie range
of mountains, although he was unable to discover any organic remains ze!
He correlated it with the Potsdam on the evidence afforded by the
Black Hills section of Dakota. The occurrence of the sandstone at Z

oe

Laramie Mountains! In opposition to the view of Dr. Hayden may —
be cited that of Mr. Arnold Hague, who states that all paleontological e
evidence obtained from the beds associated with the quartzite and _
above them tend to show that they belong to the Coal- Measure her =
stone.”

In 1871 Dr. Hayden found Obolella and.a Lingula ina sonsiderablal
thickness of Potsdam sandstone on the south side of the Sweetwater
River, near the southeastern termination of the Wind River Mountains,
thus establishing by paleontologic evidence the Upper Cambrian or —
- Potsdam age of the sandstone referred to that horizon in 1861.3

A small area of paleozoic rocks on the northwestern end of the Wind
- River range has, according to Prof. Orestes St. John, a sandstone at
the base that rests on the Archean. It is coarse rained. grayish, buff,
reddish stained, thin bedded, with oblique laminated layers and locally Fs
quartzitic. The greatest exposed thickness of this bed probably does
not exceed 50 feet. Its exact relation to the underlying Archean rock .
and to the superjacent strata referred to the Quebee was not deter- -
_mined.t On the diagrammatic section accompanying the report forma- ?
tion No. 2, or the Potsdam, is represented as resting unconformably —
upon the cnc and conformably subjacent to limestones referred t to :
‘the Quebec. :

The Cambrian strata of northwestern Wyoming are contained within ki
the district of the Teton range, Gros Ventre range, and the Buffalo
Fork Mountains, all of which are reported upon by Prof. St. John. Hee
quotes Prof. Bradley in relation to the lower quartzite, stating it to bee is ‘:
_ very compact ferruginous quartzite, with a thickness of from 50 to ‘
-feet. Above this occurs about 300 feet of sandstone strata on the

s

‘i ae a

=

ieee oa lad oualeee a et

ass

£

ee
ry
;
4
*

1 Hayden, F, V.: The Primordial Sandstone of the Rocky Mountains in the Northwestern Territork
of the United States. Am. Jour. Sci., 2d series, vol. 33, 1862, pp. 70, 71. we a
2Descriptive Geology. U.S. Geol. Expl. of the Fortieth Par. ; vol. 2. Wasldinetnas 1877, p. 18. =)

3Report of F. V. Hayden (on the geological survey of Wyoming) U.S. Geol. Surv. % the Torr, a4
4th Ann. Rep., 1871, p. 33.

“Report on the geology of the Wind River district, U.S, Geol. Surv. of the Terr., 12th Ann. Rep a
“eh 253, < “i

i ee eres ah “Se iG er ECE cae, A ee Coe sy ae
we: gh BLE 8 Fe TES Pat eae

iat - SUMMARY—CoLORADO. Ne Ee. OO

Ow

hig 1er @aldpes of the isountain’, according to Prof. Bradley, in the Teton
range. The same series of deposits evidently occurs in the Gros Ventre |
range, and in the Buffalo Fork Peak uplift. In the Gros Ventre range
the quartzites were seen in immediate contact with the unconformable
- Archean schists. _ ?
The superjacent limestone, called the “ Lower Quebec limestone” by
a Prof. St. John, occurs in the Teton range and the Gros Ventre. But .
cit is in Buffalo Fork Peak that the best section was obtained. Here
there is an exposed thickness of from 50 to 75 feet of bluish and dark
_ drab, brecciated, thin bedded, rough weathering limestone, above which
f ea ehe what he calls the passage beds to the “ Upper Quebec limestone.”
These beds are yellowish, arenaceous, micaceous clay, with indurated
— Jayers charged with a small orbiculoid shell and thin layers of dirty drab
3 limestone, the weathered surfaces of which are crowded with the frag-
. ‘Inentary remains of trilobites and other fossils. Among others there have
been identified the genera Conocoryphe and Dikelocephalus. The
upper portion of the deposit is here composed of bluish drab shales and
3 brownish gray sShaly sandstones. It reaches a BEGpaies thickness be- _
tween 100 and 200 feet. }
_ The superjacent limestone called the “Upper Quebec limestone” __
er shows almost the same development in the Teton and Gros Ventre __
3 ranges and the Mount Putnam area of Idaho. The rock consists of
generally thin bedded, fragmentary, sometimes brecciated limestones,
= color gray, grayish buff, and pinkish, carrying small sized trilobites and
Bo gasteropod resembling Raphistoma. In the Teton range the series
a _of rocks has a thickness of 100 feet or more, and forms mural exposures
_ on the.cafion walls.
A review of the reports of Messrs. Bradley and St. John shows that
_ the Upper Cambrian horizon is to be recognized in the Teton, Gros
- Ventre, and Buffalo Peak Mountains, and that it is composed of a basal
j zone of varying thickness, upon which rests a limestone carrying Up-

per Cambrian fossils. This limestone is the equivalent of the “* Lower~
__ Quebec” of Prof. St. John’s section. His “ Upper Quebec” is to be

_ referred to the base of the Lower Silurian (Ordovician) or correspond-

“ing to the Calciferous zone of the New York section.

COLORADO.

The identification of rocks of Cambrian age in Colorado has been
made, with one exception, upon stratigraphic and lithologic evidence. _
B The exceptional instance is that mentioned by Mr.S. F. Emmons, who |
| found a distinctly Upper Cambrian genus, Dikelocephalus, ina bed of —
greenish chloritic shale that he assumed to occur above the main body
ie of the quartzite and near the base of the transition series that passvs

: Ssh of the ee field work of the Teton division. U,S, Geol. Sur. of the Terr., 11th Ann,

as Ba
B52.

into the aati limestone.’ _ He describes the eine inthe Mosq
- range referred provisionally to the Cambrian as follows: ;

were
o

Bee - The beds assigned provisorily to this horizon * * * are pica
quartzite. To them, therefore, the local name of Lower Quartzite has been given.

OE - There average thickness is about 150 feet to 200 feet, of which the lower 100 feet are
- - . composed of finely and rather thinly bedded white saccharoidal quartzites, while the
upper 50 feet are shaly in character and more or less argillaceous and calcareous,

__—s passing by almost imperceptible transition into the siliceous limestone of the Siluriar
- formation above. % ae
ne “= At the very base of the series, at the contact with the underlying Archean, wherever
he this could be observed, is found a persistent bed of fine grained conglomerate, from
. afew inches to a foot in thickness, made up of rounded and finely polished grains of
- bluish translucent quartz, generally not larger than a pea in size. Above this is »
white quartzite of remarkably uniform and persistent character, always very readily

distinguishable as a white band in the numerous sections offered by the cation walls”
a

Neste? eB ie ae

of the range. Its thickness, when measured on the west side of the range or near the
Sawatch Island, is, as mentioned above, 100 feet of purely siliceous beds. On the eas
_.* — side of the range the thickness seems somewhat to diminish, and in places was fount 1
to be only 40 feet. * * * , e
eS Owing to their similar lithological character and to the general absence of fossil |
evidence it is difficult to establish a hard and fast line between this and the succeed-—
‘ing formation above. In practice the line has been drawn at the top of the shaly ;
ore Aeds, and the commencement of the beds of. more massive limestone. The transitior 4
-. __ beas consist essentially of alternating bands of calcareous quartzite and shales. The
‘name sandy limestones is often applied to them for the reason that on weathered —
surfaces of the cliff faces they appear like sandstones, the carbonate of lime having

been entirely washed out, and only the fine quartz gt aap left on the thin sua ce

Be: crust. ,

*

a ;

| As already stated, the only fossil remains found in this series occur’
- ina bed of greenish chloritic shales on the east flank of Quandary Peal kK ky.
aE t about a mile above the Monte Cristo mine. They belong to the genus”
Dikelocephalus, and closely resemble Dikelocephalus minnesotensis of

the Potsdam formation of Wisconsin. This band of shales was not

- found in stratigraphic relation to the quartzite of the limestone of the
sections already mentioned, but it occurs above a heavy white quartz-
ite and beneath a bed of white marbleized limestone; and, from anal

ogy with other sections, Mr. Emmons thinks it safe is assume that i it
occurs above the main body of quartzite end near the base of the tran -

~ ition series.°
For the purpose of comparison, a section was measured by Mr. Whit

- - man Cross, in William’s Caiion, near Manitou Springs. Of this section
Mr. Emmons says:

pa The purely siliceous beds at the base are much thinner than in the Mosquito Rang
2, the greatest thickness found being 50 feet. They are succeeded by calcareous s a 1- i

stones and shales of variegated colors, red prevailing, which pass up into white 0
drab limestones, sometimes containing chert secretions and alternating with sha ly
- beds, with an aggregate thickness of about 200 feet. These beds may be considered a:

me equivalents of the lower quartzite and white limestone of the Mosquito Ranges 4 E:

a ial i alge

rus
* Wong

=

pare

val OR

ra 1 Geology and mining industry of Leadville, Colorado, U.S, Geol, Surv., Monograph, vol: 12, 188
p60. 2
- . -- 8 Op. cit., pp. 58, 59, ie _ 0p. cit., p, 60.

rab ed fossils from a reddish rover sandstone, 45 font atove the
Lre! hean, among which an elongate form of Lingulepis, allied to L. pin-
aformis of the Potsdam sandstone of Wisconsin, occurs. From the
‘calcareous sandstones, alternating with white scateud; 105 to 122
above the Archean, the fauna is the type of that of the lower por-
n of the Lower Silurian (Ordovician).

5 ~ Two sections measured on Trout Creek by Dr. A. ©. Peale Gaye the
fo lowing results : rs

: No. 4 No. 5
een , Feet Feet
Ea Mi toh da RS casa cams . 4 daar Som ewe pees pred salccuetunbuteeicwh cone
DPE MOMEMGMSLOMOs..f.50.0...¢ 5000.0. ce5 ooo ce lea i oe gt eo at
NE OSES ae ech ane fey Lene We tes 65
. Dark, murpush: brown Sandstone ...2...2-.-... 2.202 -.5.eke 16 13
5. | Green Rt sw i waa heen wacde gee ualdns 4 3
jood-red calcareous sandstony........--.. 2.2 ee eee eee eee 2
“A 7. Pink limestones oo SECRETS RS EGC DOD RRS AGA Se eS | ae OO;

=

4 « Beds No. 6 and 7 are fossiliferous and belon g in all probability to
the Quebec group, while the sandstones below are Potsdam.” A list
of fossils is given as coming from No. 7 which indicates a grouping of
Cambrian and Silurian (Ordovician) genera unknown elsewhere.

_ Dr. F, M. Endlich’s synopsis of the rocks of the Potsdam group found
in Colorado sums up all that was known to him of the principal local-
ities and the character and thickness of the strata. Seven localities
are mentioned, as follows :? .

s Ss

~

Feet.
ihine Creek ........-. -| White sandstone and quartzite............. 250
| Bagle River..........,.| White quartzites ...............2.. ae at 300 to 400
Four-mile Creek -.......| Red and pink sandstones and quartzites.... 160
> | Trout Creek............| Yellow and pink sandstones............ 2... 80 ©
\ North of Mount Reet --| White and pink quartzites..---...........-. 200
s | Near Canyon City .--- -. Variegated micaceous and calcareous sand- |-.-. - yess
‘ ep stones.
TRU TIO. twa csianna > - Red sandstones and quartrites ae opiieie ss Sa 40
Average Mummeiees OF stvahers 2. .<- 020: 2260 Seeks eis ok. 180

That the Upper Cambrian zone is represented is fairly well proved
by the Mosquito Range section and that of Trout Creek of the Colorado
' Range, and it is very probable that the sandstones correlated with the

- _

x -'Report of A.C. Peale, M.D. Geologist of the South Park Division. U.S. Geol. Surv. of the Terr.,
p Ann. Rep., 1874, p. 208.
“Report of F. M. Endlich , Geologist of the White River Division. U.S. Geol. Surv. of the Terr., 10th
Aur . Rep. , 1878; p.130.

y > ne oath Scare
Sie :

Bee lh on YS ie Sota ENG | rt AR TES a es he Saal NE RTS
ee ee ty 4 7 Rees e SA Pes Ya, at eR eye ae A ae
mes = a ag eS Pa SA, RN ea Ryker: oy,

S ii f

Sy ie
s oe xe _ SUMMARY —COLORADO, 353

- = 7% ‘pz ii: o ws
= an ee wrt e e > : 2 — >t soe : ee 2s ¥ & AS ag Se . Pr
i of 1 oe ge > na Ve wit Ly Ha ero gia;
a : 2 q a oy = an; -s -f i ay rs 3 Boat im
854 Rawat fe “THE CAMBRIA BE See ane

Ke a Potsdam really iho sient the Upper Cambrian horizon. ‘From o one
, present knowledge the Upper Cambrian zone is the only geass of thy she
: group represented in Colorado. | Pat ees =
"~The Cambrian rocks included within the States of Ostorate, 3 Wyo:
- ming, Montana, and South Dakota are of the type of those of the south-
~ ern Interior Continental, Upper Cambrian series, and consist usually 0} of f
Su big. bed of quartzite or conglomerate, resting unconformably upon he
| - Algonkian or Archean, and passing above into calcareous beds tha ut
_ frequently carry the Upper Cambrian or Potsdam fauna. This is the
ease with the formation about the Big Horn Mountains, Wind River
Mountains, and the Teton and Gros Ventre ranges of Wyoming. — In
some instances, however, as about the Black Hills, a fauna occurs in “eh °
basal sandstone similar in character to that of the St. Croix sandstone
of the upper Mississippi Valley. Traces of a fauna were found in oles

rado, at Quandary Peak, in a schistose rock that is supposed to oce
- just above the quartzite.

oot
-
i¢
-
=

- SOUTHWESTERN SUB-PROVINCE.

me: northwestern Arizona are united in one sub- -province on account of thelif
- gimilarity in stratigraphic position, general sedimentation, and eee s.

;
Bre
Phe wee? oPo~.

<a ol Sah 5 TEXAS. *

With the exception of the doubtful occurrence of the ‘Diese Cambriat
zone as a sandstone in the Organ Mountains of southwestern Texas, a as
oreo mentioned by Mr. W. P. Jenney, the Cambrian formation is, as far ¢ s
'. known, confined to the Paleozoic uplift in the central part of the State eo
te that tablodes Llano County within its central portion. ae
a. A section of the formation measured by Dr. B. ¥. Shumard in Bi :
net County, 5 miles northwest of the town of eat} iS as follows :1

ey

No. 1. —Soft, chalky limestone with well marked cretaceous fossils <t Sn skeen bees ae
Y - No. 2.—Gray and bluish gray hard limestone, of a sandy texture, in beds froma
o few inches to a foot thick, and containing Arionellus (Bathyurus?)
Saya Bath rs! depressus, Camerelia sp., Orthis coloradoensis, Orthis

No. 3. heck gray, purple, and greenish, ‘earthy and suberystalline jimeabaneee
with alternating bands of bilsepae limestoné—contains the same fossils — G

See Be NG Boi ede So ace tee ke ew cde Se ee oseh- cee 5
“. - No. 4.—Siope with projecting ledges of No.3. ..---.-.--..-..- | Save Pa ap £0 ee
ee Wig) BLOG Jor! ia ia, oe Soe a oes en se ete Mee ERS WS Se a omadad Borer tre
No. 6.—Schistose coarse textured limestone, made up of crystalline particles and
abounding with fragments of trilobites, chiefly Arionellus ...-....---. 20

DOVES < 28 04. nies Nap vow a bacon Sie eke er eh cate ta:

1The Primordial zone of Texas, with descriptions of new fossils. Am. Jour, Sci., 2d ser., ey a2 as 7 3
p- 216, roa

- SUMMARY —TEXAS, St ee ee

Feet

Be ccceicats EU MSE MELA OGG oo ame gcc ae, Je ones, tu Smetind sev es anes 110
2.—Slope, covered with conglomerate, composed of pebbles of san dstone and

ie -ealciferous sandrock, rather firmly cemented. ......-... .--s0.----. 2-5 12

N Yo. 3.—Potsdam sandstone, consisting of thin layers of variegated green, gray,
2 ay and purplish sandy limestone, with bands of dolomite and silico-cal- |
ibe 4 ¢ i - eareous rock interstratified. Some of the beds are hi ghly charged with
_* trilobites, of which the most cominon are Arionellus texanus, Dikeloce- _
_— phalus roemeri, and Conocephalites billingsi .....-+-------------------+- 40
4.—Highly ferruginous siliceous sandstone, composed of fine grains, loosely
cemented, passing downwards into coarse gritstone and conglomerate.
The upper beds confain Lingula and Obolus (?).-.....----.---.--..---- 60

No. . Be —Flesh colored granite, interstratified with veins of milky quartz........ $: 0

~
=

a
-
AN
= *h

iy
oO. :

2
Am,

.
x
9

a

ee - From the sections it will be observed that the strata consist largely —
of limestone, with a bed of sandstone at the base.

The section of Packsaddle Mountain, in Llano County, in the valley
of Honey Creek, is given as follows by Mr. C. D. Walcott in 1884:2 ~

x St Pa 2 Feet. ;
ey - = Potsdam limestone..--...----.-----.---+------+----+ +--+ 60 ; we
pane a= Oleda sandstone. ..-........ .-=-.-.-+.-- a = eh 30 aint
Semmes Otedam limestone... .-. 0226 1.2225 sees ees hee bonnes 310 /
——— 2=—Massive Potsdam satidstone .........2.-..----. 0. +-- oe se 205 es
-1= Llano group.
605 :

S ~The fauna collected included 12 genera and 25 species, all character-
istic of the Upper Cambrian zone.

A .comparison of the Texas section with that of the Grand Cation of
the Colorado, in northern Arizona, leads to the conclusion that they
“belong to the same area of sedimentation. In each a massive sand-
stone at the base is subjacent to alternating sandstones and limestones
that carry essentially the same fauna. The sections of the lower sand-
stones of the eastern slopes of the Rocky Mountains partake somewhat
of this character, especially those of the Big Horn range in Wyoming.
In Wisconsin, ete., the calcareous beds of the Texas section are absent,
“but the presence of the Dikelocephalus fauna at the summit of each
series above a zone carrying what may be called the Ptychoparia minor
fauna, proves that thé life of the two areas continued on in the same
succession despite the change in sedimentation and environment.

* Ina report on the Cambrian system Prof. T. B. Comstock concludes
that at least two and probably three series of Cambrian strata are
represented i in central Texas.? To the basal beds he gives the name
pew series (Lower Cambrian?). For the second horizon the name
iley” series (Middle Cambrian 2), and for the upper series the name

<=
Op. cit., p. 217. .

2Note on Paleozoic rocks of central Texas. Am. Jour. Sci., 3d ser., vol. 28, 1884, p. 432.

e sor preliminary report on the geology of the central mineral region of Texas, Ist Aun, Rep. Geol,
eo oesn't toe 1889~ 90, pp. 285-291,_

x ~
tS

dam flags ; Division C, the Potsdam limestone.

_ sections exposed by the Grand Cafion of the Colorado and along th °)

Algonkian (Chuar) formation. Above the sandstoné there are 700 fee: |

_ Sils of the Upper Cambrian zone have been found. These include the

- They include Lingulepis, Hyolithes, and Ptychoparia.

_R. Marvine, is as follows :? . -

of this point they were still thinner, being estimated at less than 100

eo an a Nae rs Me
_ THE CAMBRIAN. —

_—

Katemey (Potsdam) series (Upper Cambrian ‘). This ‘upper “seed i
divided into Division A, the Potsdam sandstone ; Division B, the Pots

_-

— = —

ARIZONA.

Smee ree
nee |” ph “Pad f
ee) ee pe oe

‘As far as known the Cambrian rocks of Arizona are confined to th e
‘southwestern margin of the great Colorado Caton plateau. 3
A section measured near the head of the Grand Cajon has 300 feet
of sandstone at the base that rests unconformably upon the subjacent.

‘

of alternating sandstones, shales, and limestones throughout which fos:
‘genera Cruziana, Lingulepis, Iphidea, and Ptychoparia. At thesumm: it
of the lower sandstone a small group of fossils was found which ineludes
the genera Olenoides, Ptychoparia, Lingulepis, and Leperditia. The
upper part shows close relation to that of the Potsdam sandstone hori-
zon of central Nevada, the Mississippi Valley, and New York, while
that of the lower zone or the summit of the sandstone is more nearly
related to that of the MiddJle Cambrian zone of the Southern App
lachians. There is a large quantity of material in the laboratory of te
U.S. Geological Survey yet remaining to be studied, but I think thes
conclusions will not be materially changed. > 4
At the mouth of Kanab Creek, west of the Kaibab Plateau, there are
100 feet of arenaceous and micaceous shales, subjacent to a massive
stratum of mottled limestone. In the lower 450 feet of the latter and’
in the arenaceous shale fossils were found similar in character to those Cy
of the upper portion of the section, as seen near the head of the cafio D.

The section at the mouth of the Grand Cafion, as given by Mr. A

Feet.
Red wall limestones. . = ee
Tonto marble limestones. ; &
( Green Set wel pike Sok alate wee ; Pe :
Tonto shales, --.--. ~-----+2--- Snuff-colored 3% -.'-2--\seaes Sees = 90
Peg ae OS ee ca eee sl
. Tento sandstone:. ca... 55 cee ass wet hs ee ee ee 80 -
GEAR case Bo owe News en an aen Sefeeed Masein aie decse aap aeee See

Mr. Marvine says that in going southward from the mouth of iti
cafion the Tonto shales seem to diminish in thickness, and at Tinnakah
Springs they are estimated at less than 400 feet. A few miles south

feet.. The Tonto sandstone, however, has increased much in thickness
and forms the greater portion of the section. - |

4 Report on the geology of route from St. George, Utah, to Gila River, Arizona, examined in 187 | }
Rep. on Geog. and Geol. Expl. and Sury. west of 100th merid., in charge of Lieut. Geo. M. Wheel eler,
yol. 3, Geology, 1875, p. 199. ~ 5 -

“S

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SdOWILNG JOWIUNS Ad NMOHS SV ViWuls NVIYSWY‘) : Thee \ = |

a * 3H1 40

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SIDNIAON 1VDINOTOSD AG NOILNGINLSIG

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: - T \ |
\ : om \
at , } i

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wv

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20S

I"ld 18'ON NILATION ees a

————
|
|
|
|

‘“AMANNS 'IVIISOTOAD'S

‘tea,

(wi nicl nba Gidladba the Tonto formation) is represented as extending
from the head of the Grand Caiion along the entire course of the canon
to its mouth, and thence southward along the western margin of the
; Colorado plateau to Music Mountain, where the outcrop broadens out
and extends southwest along the south-
western margin ofthe plateau. The most y
4 southeastern outcrop is on the Rio Verde

_ River near the lower end of Williamtown
Valley.

: S In all the sections on the line of the
Grand Cafion and the western and south-
western margins of the Colorado Plateau
_ the Tonto sandstone rests uncomformably
upon either Algonkian or Archean rocks.
In its greatest development the formation
attains a thickness of 1,000 feet and rep-
resents the Upper Gainiiviari zone, and
_ possibly in the lower portion, the Middle
| Cambrian.

'
av
= SONS

|

v2
Ries

iv

Ss : }

RESUME.

23 ‘The sediments of this province are those
‘deposited as the sea advanced slowly upon
‘the land and distributed the débris worn
from itor brought in by tributary streams
as layers of sand along the coast line and
in an adjoining shallow sea. From Ari-
zona to Texas, to Missouri, the Black
) ‘Hills, and the eastern margin of the Rocky
_Mountains, ‘and all along the northern line
‘in Minnesota, Wisconsin, Michigan, Can-
ada, and the Adirondacks of New York,
} ‘the record is the same—sandstones resting o
4 upon pre-Cambrian rocks and carrying
Bree the the same fauna. In some re-

‘II PUL I “S[q UO SUOT}0OS ET} YQVONOG SLOqaINU AZI];VOO] OY 07 pUOdseaIOdD SUOTOOS OY} TYYVOTIEG s10q
"(OUT OF} OF 90) 0OBZ'D ‘O/VOS [VO]JA9A) LOPAOd UAT JOU 891 MO ‘VOULAOIg [VJMONTYMOD LOTLO}UY OT} Jo SMONIIG—"F “OL

gions the depth of water increased more
rapidly and calcareous deposits accumu-
' lated upon the sand, as in Arizona, Texas,
tl e Black” Hills, and in some localities
along the eastern base of the xia

“tana oy,

t 1e on x Hills, the eastern front of the Rocky ‘eubaeed and far’ to
the south in Texas and Arizona. All over this broad area the rela-

ee eS ae wr % oS ee ae ‘3 » ie “sat in
Bie sonlp pts os Pee ene eRe ee See
e * ; ie ct es 3 4 Lege S i = ss 4 . 3
9 ? oe > ea 6
908 0% SPs ; THE ‘CAMBRIAN. Sect eee
/ Ts 4

_ Fic. 5.—Sections of the Interior Continental Were also planed away by the Cam-

tive stratigraphic succession a ie sub: aiisiaaie oft the Upper Ca m-

brian fauna is the same; and nowhere ‘do we know of the existence of ;
- formations characterized by the Lower and Middle Cambrian faunas

=

of the Atlantic coast, Appalachian and Rocky Mountain prov ‘inces 35
except, perhaps, the Middle Cambrian faunai in the southwestern Interior
Continental sub-Province. a

In the Atlantic Coast Province the basal beds of the Olenellus. zone
rest unconformably upon Archean and Algonkian rocks. The sea de-
_ posited the Cambrian ath See across the upturned edges of the Lau-
Bat -rentian and those of the superjacent
bedded sandstones, quartzites, argil-
lites, and slates forming the Algon-
init series, which Dr. Murray referred.
to the Huronian. The upper St.
John’s slates earrying the Aspidella

Province, in the south central and south- brian Sea. Inthe Interior Continental :
western portions.
: ‘Province in Wisconsin and Minnesota

the Gagch Cambrian sandstones are unconformably superjacent to the
Jee Keaconting series of rocks, or the Laurentian, Huronian, and
-Keweenawan series of the Lake Superior region. In the first instanc e
- the earlier Cambrian sea transgressed upon the pre-Cambrian rocks, and
in the latter case the later or closing epoch of the Cambrian was the
one in which the deposits were accumulated upon the Archean and
_ Algonkian rocks. A misapprehension of these facts-has led ap L
geologists to refer the Keweenawan and other pre- -Cambrian rocks t
_ the Cambrian. | : :

DESCRIPTION OF PLATE I. ‘3

ae

Geographic distribution of the Cambrian strata shown by surface outcrops in Noe
America. sf

‘The geologic provinces are indicated by the dotted lines. The Interior Continental .
Province is broken up into sub- -provinces and these are united hy a lighter dotted
line. The provinces are: -

A.—Atlantic or Eastern Border Province. = ;
a. Eastern or Nova Scotia Basin. : ~

-b. Southeastern Newfoundland, eastern New Brunswick, and Massachw

setts Basin. : Ce

ce. Interior deposits of Gaspé, Quebec, Maio New Haurpaney Vermont, :

and Massachusetts.

B.—Appalachian or Interior Eastern Border Province.

C.—Rocky Mountain or Western Border Province.

D.—Interior Continental Province.

D!. Central Interior or Upper Mississippi and Missouri.

D*. Eastern Interior or Adirondack of New York, aud Canada.
D*. Western Interior or Dakota, Wyoming, ete.

D*. Southwestern Interior or Arizona and Texas,

The outlines of the provinces are drawn so as to include the outcrops known 3
present. They are arbitrarily assumed, as we do sg know the axpet limits of t
original Cambrian sedimentation, :

~~

o

ae
~ > * . . af 7 . a mS te 4 a
7

: pa y ee dorth into iaiad: the indicated areas upon the map
srizontal 1 black lines to distinguish caer ere the Enown Cambrian rocks.

fii _ SYNOPSIS OF THE CAMBRIAN GROUP.

¢ *

aon by Dr. i. 8 Hunt and used by Sir J. W. Dawson in 1872,
1 the Fortieth Parallel Survey in 1878, Le Conte’s Elements of Geol-
e 1878 ‘mentions, but does not use the name in classification, and

re of quartzite beneath ; (0) in the Appalachian Prices by over

2

tril

ribution ; (d) a characteristic, highly differentiated fauna.

low ring table. In some instances it is not practicable clearly to de-
(he 7 name the exact limitations of the formation through which a
eae
cer ain division of the fauna ran ges. In such cases reference will have
to be made to the text for further description.

Se pepe sis tv

vobr erate
eae Ore
-

Ne
ie

TIS

ON tia eee ee
“
*’ teeta
; | \ i -
> a! 1 .
.€ dl ar
= or" a we
E ‘
Jeet 4 er
ry att 2 :
¥ Fat * 4
‘ ‘
{ ‘ ¥ ra

-

Neem <i ay as 8 EO Be Pe pte
wat ye — oy 7 mA

pice ; Mountain province of 6 ,000 feet of i nee with 10,000 feet or -
000 feet of quartzite, Giatos slates, and limestones ; (¢) a continental

‘he e various formations referred to the group are mentioned in the

oe ea A SE NG Davy: pee en Ree ge a
ai ae OE ah Sak te RES pe RN PSG SS he Sasi
a ee AP Ras a Annee cH» 98 | ox em OS pe hat re 5 vaat ira ——. €& ;
a 7 a4 “yt Sie a oe a ts om. oy a bo ao Se as ; Ae $ ~~ ATT STE ‘ e egies
be Sag OR St 1 oe : ai ats “ “23'S eaals
\ * y A ae ea ete 5
360° THE: ‘CAMBRIAN. _ ; aunt
C * ‘ is = ry: Ss ns
. ‘ cae 9 5.05 ae $ a ; " : ohms ahs ty Rae reel eee
. iy ee Clavdipention of the Sormations. ie ESS ae

arte Toe a

=

Lower Cal. | Lower portion ‘of the Calciferous rs AES of New York and Canada; “Lowi
ciferous. . Magnesian limestone of Wisconsin, ‘Missouri, etc.

Type. =f ’ “a ®
Sandstones of the north and east sides of the Adirondacks Mountains of New ;

=
me.

3 York and adjoining parts of Canada. 4 i
| Oorrelated.
; : 3 Limestones of the south side of the Adirondacks and Dutchess wiser New r
. ‘ A York, and an unknown portion of the limestones of the ‘‘ Marble Belt” "9
; | western Vermont. e% “4
Ee 3 Potedam: He Shales of Tennessee (Knox), Georgia, and Alabama (Connasauga). - -""
tle Sandstones of the Upper Mississippi Valley (St. Croix), South Daath you
- . = ming, Montana, and Colorado. }
he, ~ Sandstones and calcareous beds of northern Arizona (Tonto) and ura Texas
y | (Katemcy).
ae J Limestones and shales of Nevada (Hamburg), Idaho, and Montane (Gallatin).
i Black shales of the i atl portion of the New Brunswick and Cape Breton
r . Island sections. .
Shales and sandstones of Conception Bay, Newfoundland (Belle Isle).
. | te on Type. | ; yi .
E : g | Shales endl slates of eastern Massachusetts (Braintree), New Brunswick (St.
F F _ John), and eastern Newfoundland (Avalon). _ é 0
si ee & jas Acadian. Correlated. a sae oe
~- oO
es. E | Z Limestones of Dutchess County, New York (Stissing), and central portions of
5 a Tennessee and Alabama, sections (Coosa). yy
2 Tea: i msg] OES 5 of central Nevada and British Columbia (Mount Stephen). —
: ae pea Type. = okereae
3 Shales and limestones of western Vermont (Georgia) and Red Sandrock.
- | oA Correlated. S
| Quartzite of western slope of Green Mountains (‘‘ Granular Quartz”) and Ap-
mee | palachian Range of Pennsylvania, Virginia, Tennessee (Chime eh Georgia,
. | 8 | and Alabama. “ee
* | 5 Shales with interbedded limestones and rooting slates of southern Vermont, _
a ? | E irrien New York, and south to Alabama. — ‘
Poles oA | Limestone, sandstone, and shales of Straits of Belle Isle (Labrador), northwest”
: Aa, 4 } coast of Newfoundland, and peninsula of Avalon (Placentia). ioe cae 4
i Basal series of Hanford Brook Section, Caton’s Island, etc., wow Brunswick
. ) | (Hanford).
* i Shales and limestones of ca ae and poutheasters Massachusetts (Attlebor-
ig aa | ough). x
Lower portion of Eureka and Highland Ranges, Nevada (Prospect).
e - | Portion of Wasatch Cambrian section (Cottonwood). ‘
l { Base of Castle Mountain limestone, British Columbia (Castle Mountain):
: } > er
: 3 ae
~ Se aes
.~ ro ns o a”

« _f I+ .
1) eg
7? Px aR
ait aS
dace yom
en eet?
ee I
ey i
4 Se
q
3 =
sy
tor ee a.
Pa ~*~ Or
on gk ae
* yee Pa]

Cambria

‘

\

q

i"

Newfoundland.

Olenus zone.

A

fi’

i Py
eA
S

fy .

Massachusetts.

Unknown.

i

f

Olenellus zones. | Olenellus zones. -

,
‘

_ New York.

=

- Table showing the order of success

Y

ion of the Cambrian faunas in typical areas in America.

Tennessee.

Dikelocephalus | Present.

zones.

7

—

by

Paradoxides zones. Paradoxideszones.| Indicated byother|} Represented by | Represented by. Represented by | Unknown,

\

: *.

N

_

Nevada and Utah. | British Columbia.

Dikelocephalus | Not recognized,
but probably
present.

zones.

——

geperathanPar-| other genera other genera other genera
adoxides. _ than Paradox- than Paradox- than Paradox-
' | ides. i ides. _ | ides.
c i}

- t
=|

Olenellus zones.

Olenellus zones.
Hick

>|
a fa

Olenell

~

lS —

Valley.

Dikelocephalus
zones, —

oS
us zones. | Olenellus zones. | Unknown. |
ot ‘

Upper Mississippi | Texas and Ari-

*

zona,

Dikeloc ephalus
zones.

Not determined.

\ ¢

*

4 ee

Unknown, ~
- 71

_

™~

=

Re i Soke - aaa - hes ee SS Malt lee See it OA ne en er

: : i
5 * ’ ; - ‘ se
7 re Mm < ~i t ray : a, tee »
% 4 ~ oom 2, = . ox , Ss - al ga ; oC, S
as : = hl alt Ts ues = oe
. > ‘ +o , , stasis > - 2 ‘

} Province, but in the Lake Champlain Valley and the Southern Appall

_ illustrations of this is in the Eureka district of Central Nevada, where, ©

: , rte"
fe: ae (ess, ¢ on id 5 Ee
‘ PEAS s 2 — ap”
4 = ooh : = me, % i J

«
a

BASE OF CAMBRIAN. Lg Sees a

— es .. - eee

- The statements acta in 1 the preceding pacaEhEG RE: foreshadow 1 the
_ conclusion that over the Interior Continental area the basal beds of t
upper division of the group rest unconformably upon pre- ‘Cambria an
rocks. This is true also of the lower division of the Atlantic Coa st

chian Province there is no positive assurance that the conformable se-
ries of strata beneath the Olenellus zone do not pass down into some
pre-Cambrian group. In Nevada, Utah, Montana, and British Colut n-
bia the same conditions exist to a more macknd degree, and I have, ir
the absence of paleontologic proof, referred the conformable pre-Olene ;
Jus strata to an Algonkian group. Thata considerable portion if nota
of the series will be ultimately referred to the Cambrian is probable
from the fact that the Olenellus fauna has been traced downwaré dd
through 1,000 feet of limestone in the Champlain Valley of Vermont and
3,900 feet dow aware in the Bow River series of British Columbia. The
great vertical distribution of the fauna in the limestone leads to the ex ;
pectation that it will be found to range through a considerable portion
of the conformable strata beneath the narrow Olenellus zone of the
Southern Appalachian and southern portion of the Kocky Mountain
Province. On the map of sections the lower strata are provisionally y
and doubtfully referred to the Cambrian. This is in opposition to the
view advanced in the Tenth Annual tc oh of the U. 8S. Geologica al
Survey. | a
| SUMMIT OF CAMBRIAN. ) eae
The determination of the top of the Cambrian is beset with more dif.

- ficulties than its delimitation at the base. At the base there are marked
-unconformities, and in their absence the presence of a distinctly marke od
fauna beneath which no other fauna has yet been found. At the sum-
mit, however, we meet with a transition both in sedimentation and fauna:
to the characteristic type of the Silurian (Ordovician). Oneof the best. |

in the Pogonip limestone, the passage from the Cambrian to the Silurian
(Ordovician) is so gradual that it is only by the predominance of the e
fauna of one or the other of the two great groups that a line of demarka-
tion can be drawn. The transition is such as might be expected wher é
there was no marked physical disturbance to influence the change of
_ faunas resulting from the natural dying out and development of species
or the influx of new species from other areas. The sedimentation was
very uniform, and no essential change of character occurs between the e
_ limestones of the Upper Cambrian and those of the Silurian (Ordovician).
On the other hand, the delimitation between the two groups on the
northern side of the Adirondacks is clearly and definitely marked by the
occurrence of a light-colored, calciferous sandrock, with its distinctive
fauna, resting at a compact, hard porary, characterized by ¢

Mer a

ae
3.3m
Pn ws >? *

lo os ina fauna of the iisper Oambsini, Various grades of tran-
} oer between these two extremes, but frequently it is necessary
raw an arbitrary line and define the upper limit of the Cambrian, as
rinating where, in any continuous section, the Upper Cambrian fauna
rives way, and is superseded by the types of the Siluriau (Ordovician)

& mestone; in Tennessee, near the base of the Knox dolomite; in north-
ern} New York, north of the Adirondacks, between the Potsdam sandstone
and the Calciferous sandrock ; on the south side of the Adirondacks, in
t the limestone between the Potsdam and Calciferous faunas; in the Up-
- per Mississippi Valley, between the upper beds of the St. Croix sand-
stone and the Lower Magnesian limestone, or in some instances in the
lower portion of the Lower Magnesian limestone; in the series of shales
2 opposite Quebec, at Point Levis, beneath the graptolitic-bearing shales
a and the conglomerate carrying the Dikelocephalus fauna of the Upper
Cambrian ; and in western Newfoundland, in the limestones between
the. Gnper: Cambrian fauna and the base of the Ordovician fauna.

= The paleontologic break between the Cambrian and Silurian groups
is practically complete where the stratigraphic break is marked. About
a ‘the Adirondacks the only species I know of that cross the break are
J the Lingulepis acuminata and a species of Ophileta, at Chateaugay
Ss Chasm. In Wisconsin some of the species of the Upper Cambrian fauna
_ apparently rise into the lower portion of the Lower Magnesian lime.
‘aa stone, and are there associated with forms which are considered to be
: more typical of the. Silurian (Ordovician) fauna. In Nevada, where the
‘ sedimentation is of the same character in the Upper Cambrian and the
_ lower portion of the Silurian (Ordovician), there is a slight blending of
~ the faunas, as shown by the occurrence of the genera Asaphus, Dikelo-
Se sigina, and Ptychoparia upon the same surface of rock. With our
_ present knowledge, however, the occurrence of the same species in
- strata that are referred to the Cambrian and the Lower Silurian is so
- rare that they are the exceptions to the general rule.

J

it is not, however, by the specific break in the fauna that the two

groups are Mpaiatod, ; it is the general facies of the fauna referred to
the Cambrian and that referred to the Silurian (Ordovician). The dis-
tinctness of the Upper Cambrian fauna from the Lower Silurian fauna
100 feet beneath the line of contact of the two groups is such that I
~ think there will be no confusion between the two faunas in America.
) In England the range of the genus Agnostus has complicated the sep-
~ arateness of the two faunas, but this is not sufficient to combine them
asa whole.

er}
—

SEDIMENTATION OF THE CAMBRIAN GROUP.

- Se physical and lithologic characters of the strata lead to the con-
- elusion that the sediments were accumulated in relatively shallow seas

slowly - depressed in ‘relation to the surrounding waters. There are

SYNOPSIS. Mires 363

‘una. In Nevada this line would be drawn near the base of the Pogonip

int the immediate vicinity of the shores of land areas that were being:

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‘ gome Seat as, for instance, the deeper water acetone series ¢ of
central Nevada, British Columbia, and western Vermont, and pe r
haps the black shales of the Atlantic Coast Province. The assembled

evidence sustains the view that at the beginning of Lower Cambrian
time the area of the great Interior Province formed part of a continent,
to the eastward and westward of which long ridges of pre-Cambrian
rock separated interior seas and straits from the continental area and
protected their contained life and sediments from the ravages of the

Open ocean. As the continent was slowly depressed and the waters
advanced upon the land the sediments now fo rming the rocks of the
Lower and Middle Cambrian series were accumulated in the various
interior bodies of water to the eastward and westward of the main
land area and between it and the outlying ridges. What the contour

of the south and southeastern side of the continent was and to
what extent the sea advanced upon it from the south during this ©
time is unknown and may never be known, as only the formations
that were deposited around the pre-Cambrian islands of Texas and—

‘Missouri are now accessible for study. From the evidence afforded
by these two localities and that along the eastern front of the Rocky
Mountains, and the exposures of Cambrian strata in Wisconsin, Can-
ada, etc., it is very probable that the main portion of the continent

north of the thirtieth and south of the fiftieth meridian did not dis-
_. . appear beneath the advancing sea until near the beginning of Upper

Cambrian time. The unconformable position of the Upper Cambrian —

rocks of the Interior Continental Province upon the subjacent Algon- |

kian and Archean rocks sustains this conclusion. 3

As the sea was transgressing over the surface of the continent on
its way northward across the broad interior in late Middle or early

Upper Cambrian time it was also working along the base of the border~

ridges and depositing the sediments derived from them conformably
upon those deposited, while the main mass of the continent was above —
the water. That these deposits were practically contemporaneous with.
those of the Interior Province is proved by the presence of the same ~
types of animal life, and to a considerable extent of identical species. —

- Toward the close of Cambrian time a large portion of the continent —
had disappeared beneath the surface of the sea, and the great lime- —
~ stone-forming period of the Silurian (Ordovician) began. In some
areas, as about the Adirondack Mountains of New York, argillaceous —
and arenaceous sediments were derived from the adjoining coast line,
but as a whole mechanical sediments are absent. — = ‘a
1In speaking of the conditions of sedimentation Messrs. Campbell and Ruffner state that “Changes. |
such as these occurred, during a series of geological ages of unknown length, in a great inland sea 9
which was once connected with what is now the Gulf of Mexico, on the south; limited probably by
the highlands of Canada on the northeast, having the Archean ledges of the Blue Ridge for its
southeastern border, and in all probability separated, in part at least, fromthe Pacific Ocean by the
. Rocky Mountain Range. This extensive sea, with Archean rocks for its bottom and shores, was the —
receptacle of the various materials that now constitute the surface rocks and soils of the Mississippi _

Valley.” (A physical survey extending from Atlanta, Georgia, across Alabama and Mississippi to —
the Mississippi River, along the line of the Georgia Pacific Railway. New York, 1883, pp. 9, 10.) PS ‘3

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_ SYNOPSIS. 365
Bercetotion had pet an immense amount of material
th » advancing sea to assort and rearrange in early Cambrian time.

is, with that worn from the solid rocks by the attack upon the coast
e, was largely disposed of prior to the opening of the limestone-
forming period—an epoch varying in relative time in the various
| "provinces.

Lae do not think it probable that any Se EY amount of sediment
accumulated i in the southern portion of the Interior Continental area dur-
“ing. early Cambrian time. The sections of the Champlain Valley, eastern
: Tennessee, Utah and Nevada, and of British Columbia prove the accu-
% mulation of from 10,000 to 12,000 feet of sediment along the eastern and

"western flanks of the pre- Chegibrinn continent before the sea deposited

_tlie formations about the Llano Hills of Texas, the Ozark Mountains of
— and other portions of the Interior Continental Province. This
> vidence leads to the belief that the continent stood at a considerable
levation, and that the great accumulation of sediment during late
Algonkian and early- Cambrian time resulted from the distribution of
material worn from the shore by the waves and brought into the sea by
“the rivers of the Interior Continental region and the outlying ridges.

a Ce DESCRIPTION OF PLATE IL.
:

M Map of the central portion of the North American continent, to illustrate the rela-
tiv e thickness ‘of the strata composing the Cambrian group in the various geologic
"provinces. (The small ring with the dot in the center indicates the geographic loca-
tion of the base of the section.)
a The sections are grouped into the following geologic provinces: . ‘

H
4

ia _ Atlantic Coast Province.

¢ Appalachian Province.

iy Rocky Mountain Province. 3
__- Interior Continental Province.

;
The latter consists of the Central Interior or Upper Mississippi, the Western or
= ocky Mountain, the Southwestern or Arizona and Texas, and the Eastern or Adi-
;
- rondack sub-provinces.
_ ATEANTIC COAST PROVINCE:
4 SECTION 1. Conception Bay, Avalon Peninsula, Newfoundland.—The Cambrian rocks
is of the Avalon Peninsula rest unconformably upon strata of Archean and Algonkian
F age. The section represented is formed by the union of portions of those of Manuel’s
k Brook, Kelly’s, Great Bell, and Little Bell Islands.

+ SECTION 2. Vicinity of St. John, New Brunswick.—This section is unconformably
_superjacent to the Archean, and unites the section at the city of St. John and that
4 of Hanford’s Brook.

{ ‘It is not improbable that the area of the great coastal plain of the Atlantic slope was then an ele-
N ated portion of the continent and that much of the sediment deposited during Cambrian and later
Paleozoic time was washed from it into the seas im mediately to the west. Ifthis be true the source
y: posits of the eastern coast line is explained by the sinking of the coastal region during, or at the
_ lose of Paleozoic time. This view is strengthened by the presence, in the Middle Cambrian fauna
of Alabama, ofa number of speciés that are closely allied to if not identical with species of the Mid-
die Cambrian fauna of Newfoundland and Sweden. This fauna is unknown in,the Appalachian Prov-
a ce north: of Alabama. This leads to the inference that it was distributed along the shore of the
tlantic Coast Province, and that the line of deposits, uniting the Newfoundland and Alabama areas,

Bi uth of the Massachusetts area, are now buried deep beneath later deposits.

of much of the sediment of the Appalachian series of rocks is accounted for and the absence of the

-

_.. superjacent to the Archean. : Se Tee Le €:

THE, ‘CAMBRIAN. 250% Se
Pee 3. Vicinity of North Attlebor ough and cnet ‘Mamaaheontis ae: is

section the Lower Cambrian series of North Attleborough and the Middle Car ymbr ane

of Braintree are united in oné generalized section. The basal series is unconformably- :

¥
_ = - a

APPALACHIAN PROVINCE: sk,
SECTION 4. North side of the Straits of Belle Isle, Lasiidioe. _The Sink rests “uncon-_
formably upon the Archean. -
SECTION 5. Central western Newfoundland.—The base rests dsjoontecinabhy seal the.
Archean, but the summit of this section is not clearly defined owing to lack of data
to determine the range of the fauna. | le
SECTION 6. Franklin County, Vermont, —This represents the ‘‘ Red sandrock ” series, —
with its superjacent Georgia shales, in the township of Georgia. The base is ous off —
by a fault line, and the exact limitation at the summit is unknown. weet)
SECTION7. This represents the great shale and slate section of Washington County,
New York. It is cut off at the base by a fault line and the summit is not well defined. |
SEvTION 8, The shore-line deposits of the Green Mountains or the “Granular |
Quartz,” above which come limestones in which Cambrian fossils have been found. —
At the base it rests unconformably upon the crystalline pre-Cambrian rocks, — -
SECTION 9. Typical section in southern Pennsylvania, showing the “ Granular
Quartz” resting unconformably upon the subjacent crystalline rocks and extending
above into the shale series beneath the limestones. 45 ls
SrcTion 10. This section is that of central Virginia, not far away facie shore
line. The base rests unconformably upon the pre- Cambrian rocks, and above it pas ASSES

_ into the base of the “ valley ” limestones. cS i : s

- fault line and above it passes into the Knox dolomite, the lower beds of which carry a
_the Upper Cambrian fauna. The Chilhowee Mountain section comes beneath the

- the hiatus between the two sections. The data for this section are given by Mr. Baileyi

division of the U. S. Geological Survey. . Bp

SECTION 11. Rogersville, East Tennessee.—The tase of this section is cut off by ¢

Rogersville, and it is so represented in this section, An interrogation point mark

Willis, chief of the Appalachian division of geology, U.S. Geological Survey. ~ ~
SecTION 12. The line of this section extends from Rome, Georgia, westward into
Alabama. At the base it is cut off by a fault and above is delimited by the Knox |

dolomite. The data for it are given by Mr. C. Willard Hayes, of the Appalachian)

SECTION 13. Western slope of the Wasatch mountains, Utah.—In this sbekine he
12,000 feet of quartzite and siliceous slates are tentatively referred to the Cambrian.
The fossiliferous zone is confined to the upper 250 feet.

SECTION 14. Central eastern Nevada.—This section represents the great quartzite
series beneath the fossiliferous Cambrian limestone. The base has been concealed,
and the summit has been removed by erosion. “=e

SecTION 15. Eureka District, Nevada.—In this section the fossiliferoua. feiss Cam-
brian strata rests conformably upon the quartzites, whick pass down some 1 900 feet b
before being concealed. The quartzites may correspond to the upper beds of section
14, The summit of the section passes into the Superjacent Fogonip limestone of the a
Silurian (Ordovician). 9

SECTION 16. Gallatin River near Gallatin , City, Montana.—This is ensontislly the
same as the Mount Stephen section of British Columbia (section 17). The sibjacedil
series of quartzites and siliceous slates are tentatively included in the Cambrian.

SECTION 17. Mount Stephen section of British Columbia, in connection with bs)
subjacent Bow River quartzite and siliceous slates. The relations of the section ar
the same as those of the Eureka section (15) of central Nevada, with the addition « of
the Bow River quartzite and slates. z

wn ee
< >

Rocky MouNTAIN PROVINCE: - ; “sd
Central Interior Centinental subprovince: -~ - 5 ot ae
SECTION 18. The western section of the central Interior Continental Provinee a

~~

~

‘jt occurs in Minnesota, ~ ‘| . 2 AS 5a 3

Oye PEC is = a>, ; eae
ct

5. = SYNOPSIS."

2 yma’

eS Bye Oe a ? ;

. “Section of the Uppéi Siesta sandstones of eastern Wisconsin.
nox 20. Section of southern central Wisconsin, showing the unconformity
n the Upper Cambrian and the subjacent Algonkian and Archean rocks. See-
: 9, and 20 are all of Upper Cambrian age, and pass conformably above into
Tt ® superjacent Lower Silurian (Ordovician) or magnesian limestones. ‘
_ SEcTION 21, Ozark Mountains, southeastern Missouri.—The relations of the Cam-
as un ana the Archean are the same as those in the Black Hills section (section 23).
_ Easteru or Adirondack subprovince:

ork,—In this section the Potsdam sandstone of the Upper Cambrian rests uncon-
formanty upon and against the Archean and Algorkian rocks.

2 hana Interior Continental or Rocky Mountain sub-province:

SECTION 23. Black Hills, Dakota.—The Upper Cambrian rests Die cok. upon
e Archean. bute de

SECTION 24. Eastern section of Big Horn Mountains of Wyoming. —It is essentially
th hé same as that of the Black Hills (section 23). .

; SECTION 25. Southern Montana. —This section is very much like that of Wyom-—
i and of the Black Hills.

_ SECTION 26. Central Colorado.—A section yeprésenting the sandstones that lie ie
ween the subjacent unconformable Archean or Algonkian rocks and the superjacent
oe. Silurian (Ordovician).

ae S Southwestern Interior Continental sub-province :

SucTION 27. Grand Cation of the Colorado, northern Arizona.—In this section the
. E Baatirian strata are uncomformably superjacent to rocks of Algonkian age.

- §xcr10N 28. Llano County, Texas.—This section is similar to that of the Grand —
-Cafion i in having an unconformity between the Algonkian 4nd the Cambrian and in
_ representing nearly the same geologic horizon.

ained from the associated map. The enormous accumulation of sediment in the
Rocky Mountain Basin on the west and the Appalachian Basin or trough on the

eas in a shown, as well as the thin mantle of sediment over the great interior. It
~ serves to illustrate the sedimentation indicated by the oe columns on the map.

a oun knowledge of the sediments of the eastern and western sides of
» pre-Cambrian continent is considerable, but of that deposited along
th the southward-facing front we know nothing. From the fact, how-
iy that the same species of fossils occur in the Lower Cambria
auna of Labrador, Massachusetts, New York, Vermont, probably
F Ponnessee, Nevada, and British Columbia, I think we may hypotheti-.
Hy assume the continuance of the Lower Cambrian beneath the de-
posits of the Gulf States and westward through Texas, New Mexico,
ao Arizona. There is no known line of Lower and Middle Cambrian
e sedimentation across the continent to the north of this which indicates
at the fauna might have been distributed along a more northern
shore. —
“the pre-Cambrian ridges, or protaxis of the present ranges of the
ortheastern. side of the continent, have been outlined by Prof. J. D.
Ds na from the known exposures of pre-Cambrian rocks.!. The Para-
oxides fauna lived in the depression between two of the eastern ridges
ofthe Atlantic Province in the New Brunswick area, and in the bays

re sof continental progress in North America and the influence of the condition of these areas on
work casi forwart within them. Bull. Geol. Soc, Am., vol. 1, 1890, pp. 36-39

_ Secrion 22. The eastern and northern slopes of the Adirondack Mountains of New :

re ieoretic sections at close of Cambrian time.—The data for these sections are ob-—

ee

and pnotented SKotes of hes ee ot oe of. the ceatort ridge, where

Re i Eee
iets pes iota
% ‘ ae

the outer or eastern ridge was absent, as in Massachusetts and New- a

foundland. The sediments that accumulated to the eastward of the -
New Brunswick sea form the supposed Cambrian shales and slates of |
Nova Scotia. The inner ridges of Maine, New Hampshire, and Massa- —
_chusetts bounded long, narrow seas, in which the Cambrian faunas are —

=

not known to have penetrated. The Lower Cambrian fauna probably —
passed from the Atlantic along the ancient Labrador shore into the 3
interior Appalachian sea. A few types of the Middle Cambrian fauna :

followed, and then the passage appears to have been closed, as none of
the Upper Cambrian types of the Atlantic fauna have nece found in
the deposits of the interior seas. <2

The various views, both theoretical and hypothetical, relating ie the —

pre-Cambrian continent are embodied on the map, PI. 111, and the sec-

tion at the base of Pl. IL. . | yw

~

DESCRIPTION OF PLATE II.

Hypothetical map of the North American Continent at the beginning of and aucthy Coneesd 4

we A

Cambrian time. —.
or.

This map is based“ upon the sections shown on Pl. 11, and the theoretic section at

the base, The position of the sections on the two maps is indicated by a circle with
a corresponding number on each map.

a
The shaded portions indicate the relative areas that are supposed to _have ‘been ;

above the ocean during later Algonkian and Lower Cambrian time. A comparison

*

-with Pl. m shows that in the Rocky Mountain and Appalachian areas there was an %

enormous accumulation of sediment prior to the Upper Cambrian; while over the 2

broad interior there is only the Upper Cambrian which corresponds to the upper por- —
tion of the great sections of the Rocky Mountain and Appalachian areas. In the

region of the Atlantic Coast Province the continental movement seems to have been —
less, as the sediments of the Lower and Middle Cambrian are much thinner than

those of the corresponding horizon in the Appalachian and Rocky Mountain areas. —

The conclusion is that the shaded portions and perhaps other unknown areas formed 4

the land during late Algonkian and early Cambrian time, and that about the close —
of the Middle Cambrian or the beginning of Upper Cambrian time the- continental
surface was largely depressed beneath the waters of the ocean and the Upper Cam-
brian sediment accumulated over the entire area where asc sd: rocks are now

~ known to occur. (See distribution on Pl. 1,)

_time there were geographic areas in which different types of sedimenta a

On PI. 111, A., Archean ; K., Keweenawan ; B. H., Black Hills of Dakota: » Llano

area of Texas; M. Orie uplift of Missouri; C., ena Cafion area of ‘meses The |

area marked X, X, x indicates an hypothetical hada area of the existence of which ~ ¥
we have not at present any absolute proof, as it is now covered by Bi ie of later
age than the Cambrian. . a

' The present shore outlines of the continent are indicated by the dotted tive: and the a

outlines of the continental plateau on the division between the deep sea and the conts 4
tinent by a continuous line. eee f ee =

o

The descriptive notes of the Cambrian rocks of the various provinces -
and the résumé following each establishes the fact that in Cambrian —

.~ oe
- on

VEY

U. S. GEOLOGICAL SUR

5 ae

x Taya,
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at the beginning of
Lower Camerian TIME
by .
C.D.WALCOTT
1891

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HYPOTHETICAL MAP
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NORTH AMERICAN CONTINENT

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ee NaS SYNOPSIS. 369
Las ie ee : M ‘

( ny re vailed, and that. great variation aeiated 1 in what are considered
he same geographic provinces. The sediments of the northeastern
Atlantic Coast Province are almost entirely shales with a small propor-
ion of sandstone and a trace of limestone. Tracing the long Appa-
r hian Province from the Gulf of St. Lawrence to the southwest and
. th, we find an immense accumulation of shale with some interbedded
an ndstone and limestone. This extends to the Lake Champlain region
‘New York and Vermout, where a great limestone of Lower Cambrian
age e is subjacent to several thousand feet of shale in which lenticular
asses of sand stone and limestone occur at irregular intervals. Farther
to the southwest, in southern Vermont and eastern New York, great
‘tl nicknesses of argillaceous sediment were deposited. These now form
tl e series of shales in which beds of finely laminated roofing slates
oc ecur in massive Strata. Toward the east, near the pre-Cambrian shore
ine, the Lower Cambrian sandstones are followed by arenaceous, dolo-
n itic, and purely calcareous limestones of later Cambrian time. This
ondition of sedimentation continues far to the south, varied more or
less by the presence of great thicknesses of shale above the lower
qu Sttzito, In the latter case the limestone of the Cambrian forms only
‘thin belt at the summit.
In the Rocky Mountain Province the siliceous sediments, sandstones,
nd quartzites are followed by limestone, and nearer the shore line,
‘the sandstones are subjacent to shale. Over the Interior Province the
record is sandstone, followed on the west and southwest by alior inlay
ti mestones and sandstones.
On the map (Pl. 11) the thickness and character of the sediment is
8 geez ina general manner for each of the provinces.
‘The study of the fauna has shown that, while there is a general re-
Beinblance in the faunas of the Lower Cambrian in the Atlantic Coast,
Appalachian, and Rocky Mountain Provinces, there is sufficient ditter
e entiation to mark off distinct faunal areas in the early Cambrian sea.
The fauna of the Upper Cambrian is less specialized over great areas
an that of the Lower and Middle zones. The opportunities for com-
peanication between the provinces were greater and it is only in the
eoteestorn or the Atlantic Coast Province that a marked difference
is shown.
- The Middle Cambrian fauna of the Atlantic Coast Province is so
‘st ongly differentiated from that of the Appalachian and Western
a Mountain Provinces that it was not until they were found to oc-
cupy the same relative stratigraphic position that it was suspected they
; ii fy ved in approximately the same epoch.
The evidence of sedimentation and the evidence of organic remains
2 nite to prove that in Cambrian time the geographic and faunal prov-
neces were differentiated and established over the area of the present
rth American continent. In fact, the sedimentation of the Cam-
dani was as varied as that of many of later geologic periods and more
th ass that of the immediately macconding Silurian (Ordovician).
“Soe S1—24 :

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SR ee NOS ae ae i ig
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- - : a - we a, at pa Sie ‘we 7 ee y
SUBDIVISION OF ‘THE CAMBRIA. “ ‘4 ~# rat iW

In his Sebi ‘report upon the Devonian of nore America Prof. |
_ H.S. Williams expresses this opinion: ~ | Fis

-

The subdivision of any great geological ‘system must depend in great mepshenl

- upon the differences in the faunas or floras contained, and, as I believe, “this depends — =

in no small degree upon the geological changes which Endod and shifted the geo- —

graphical conditions under which the animals lived. A sandstone will not ‘contain —

the same species as a following limestone, and even in arenaceous shales a slight _

change in the fineness or coarseness or in the amount of argillaceous mud mixed —
with the sand modifies the composition of the fauna contained in itt —

There are not at present sufficient available data from the Cambrian f
upon which to base comparisons with the same degree of refinement as _
those made by Prof. Williams. It has been discovered, however, that
the predominant types of life of the Cambrian group are to be found in
shales, limestones, and sandstones. For instance, the genus a
characteristic of the Lower Cambrian, is found in the shales, limestones, ;
slates, and sandy shales of the typical section in Northern Verinont.
I have found in the quartzites and in the pure limestones of the Pots- ;
dam epoch of the Adirondack subprovince the same species of Dikel-
ocephalus, Hyolithes, and Lingulepis. In the dark argillaceous shales. ;
of the Middle Cambrian terrane of Newfoundland I found the same

- species of Paradoxides that occurs in the interbedded limestones of ;
the same series a few miles distant. That Prof. Williams is correct in —
relation to the great mass of organisms <hat existed during Paleozoic :
time there can be very little if any question. Asan example the corals
of the limestones of the north shore of the Strait of Belle Isle, on~
the Labrador coast, are unknown, except in an almost identical lime-
stone at Silver Peak, Nevada, in the Rocky Mountain Province. Itis
in the clearer limestones that the great bulk of the brachiopods,
pteropods, and other forms of life are found in the Cambrian; but it is”
a fact, nevertheless, that the predominant types of the Trilobita, char-
acterizing its three divisions, flourished upon and were imbedded. in
sediments of widely different character. It is owing to this taat they !
become of so much importance as criteria in the correlation of the th |
primary divisions of the group. SS

In the Atlantic Coast Province the fauna of the Lower Cantbeianais ;
Olonellus zone, occurs in arenaceous limestones, pure limestones, and
shales. All of these are of a different character from those of the black
shales 200 feet above, in which the Paradoxides or Middle Cambrian
fauna occurs. The Upper Cambrian fauna is found in dark shales and
sandstones several hundred feet, if not a thousand feet, above the a -
doxides zone. The three primary subdivisions of the Cambrian ¢
strongly defined by the sedimentation and faunas. Inthe Bt. Lawrence ce

1 International Congress of Geologists, American Committee. Report of the subcommittee tot he
session of the Congress held in London, September 17, 1888. Philadeiphia, 1888. Report of thes
committee on the Upper Paleozoic (Devonic), H. 8. Williams, Reporter, P. C 2..,*" “<

~

= Brcrinn fanank are found in separate bands of conglomer-
mestones and not in situ, the great thickness of shales and Sand-
ae to the Uinuibrak not being characterized by any known
) tbe Vermont the eatin eran fauna occurs throughout the

hiv ay Georgia shales, while about 2,000 feet above, the Upper Cam-
‘Le ¥

brian fauna is well determined. The ‘Middle Cam!rian fauna has not
been phages nite wine eastern New York section the Lower Cam-.

¢ 5 Only: a few miles distant to the west, however, at the base of the aaa
ro: pecans, the Upper Cambrian fauna characterizes sandstones and-
nestones that occur beneath the base of the Silurian (Ordovician).
arther to the south, in Dutchess County, in the valley of the Hudson,
th e Lower Cambrian fauna is recognized in the basal quartzite and the
su perjacent limestone, and also the Middle Cambrian of the Appala-
o ae and Rocky Mountain Provinces, and the Upper Cambrian of all
yut the Atlantic Coast Province. In Tennessee, in the Southern Appa-
fl nian. Province, the Lower Cambrian fauna is found in shales, within
the , quartzite Series, and at the summit of the shales the Upper Cam-
bri ian fauna occurs. This extends up and into the base of the limestone.
n Alabama, in shales apparently occupying the same serial relation,
the Middle Cambrian fauna is well developed.
y In the Nevada section the Lower Cambrian or Olenellus zone is dis-
tinetly defined, and between it and the Upper Cambrian fauna 1,000
eee of limestone is marked by types of the Middle Cambrian fauna.
hese distinctions of faunas are readily determined wherever two or
mi pore of them are present in the same section in the Rocky Mountain
Pr rovince. In British Columbia the Lower Cambrian and Middle Cam-
brian faunas have alone been recognized.

_ Ihave spoken of the Middle Cambrian fauna of the Atlantic Coast
P ‘ovince and that of the Middle Cambrian of the Appalachian and
Ro ky Mountain Provinces. This distinction is made because the char-

i 1c! eristic types of the Atlantic Coast Middle Cambrian fauna are not
fot ound in the Middle Cambrian fauna of the other two provinces. This

:
ay
at
i

Xe upy Cake. same relations to the Lower and Upper Caneies faunas

q a, that a nad ‘impassable barrier existed Depts pe .

do es s the Middle Cam brian or Paradoxides fauna of the Atlantic Coast

Upper Cambrian with the single exception of the Atlantic Coast Prov- :

_ Alabama, Virginia, Pennsylvania, ete. Another is in the widely spread

- sandstones of pre-Cambrian and post-Cambrian age have also been

_ we find an extensive development of Cambrian rocks in North and

of North Wales and the Cerfai group of South Wales; the Middle,

si 5 Magee Sygate : | | CAMBRIAN. OR |

possible in all instances to differentiate the primary divisions of Upper, :

The Lower Cambrian ‘fauna i is much more persistent i in its cas
than that of the Middle Cambrian; for all the strata referred to ‘the 5
former horizon have been found ts be characterized by essentially
the same fauna. This is also true of the much more widely spread

ince, where the fauna is more of the European or Atlantic Basin type.
There is, however, too little known of it at present in Newfoundland
to base any final conclusions upon it. > ae

The minor or formation subdivisions of the Cambrian are based largely ;
upon lithologic characters and are relatively of local value only. One
exception to this is found in the “ Granular Quartz” of New York and

Vermont, and the equivalent Chilhowee quartzite series of Tennessee,

shore-line deposits, called the Potsdam sandstone in New York, the St.
Croix sandstone in the Upper Mississippi Valley, the supposed equiy-
alent deposits of the Black Hills of Dakota, the sandstones of the —
eastern flanks of the Rocky Mountains and of the Llano area of Texas,
These two formations furnish illustrations of the accumulation of similar
sediments over very extended areas. Their minor value in classifica-
tion, when not supported by paleontologic evidence, is shown by the
fact that the Lower Cambrian ‘Granular Quartz” or Chilhowee sand-_
stone has been correlated by nearly all geologists who have referred to
jt with the Potsdam sandstone about the Adirondacks of New York
and the St. Croix sandstone of the Upper Mississippi ‘Valley, thus.
bringing together formations separated in the stratigraphic column by
a long time interval and several thousand feet of sediment. Other

correlated with the Potsdam sandstone of New York. .
With our present knowledge of the faunas and sediments it is na

Middle, and Lower Cambrian in America.
Extending our views across to the eastern side of the Atlantic Ooehie ‘

South Wales, where the three great divisions of the North American 4
Cambrian are to be recognized. The Lower, in the roofing-slate series |

in the Solva and Menevian formations, and the Upper, in the Lingule
flags series.. These divisions are also recognized in Sweden and North
Wales, although in greatly diminished force. The Lower division has
been recognized in western Russia, and the central belt of the calebiatal ¥
‘‘ Zone Primordiale” of Bohemia represents the Middle Cambrian series.

In lithologic, stratigraphic, and paleontologic characters the Cam-
brian series on the opposite sides of the Atlantic are such that there is
no hesitancy in considering them as belonging to one geologic group 0
and as part of one geologic basin.

There is a great variation in the sedimentation and Be pink of the >

~
‘ ae ~ + rae
( ; ey: <
4 *
wy

- he
. ‘ ce 4
* / wos mo ol
. ~ , & ee SD Si

a 4
E Aimations referred to the Cambrian in North America and
; they all fall within the limits of the group and, united, consti-
‘great geologic division of equal taxonomic Gants with Silurian
: ovician), “saa Devonian, ete.

-— <.
44

cbintson WITH THE CAMBRIAN ROCKS OF OTHER COUNTRIES.

in
Co
ws ‘ai

a ae EUROPE.

Dr. Henry Hicks expresses the view that the sediments of the Cam-
sa and Silurian were largely deposited on the western side of the
Huropean continent.1_ In Spain and Wales the sediments accumulated
4% © a great thickness, while to the eastward, in Bohemia, Scandinavia,
a and Russia, the sections show less than one-fifth of the thickness of

pon the Archean. These observations lead to the conclusions (a) that
ne Cambrian sediments were deposited upon a gradually sinking coast
ae - (b) en the greatest depression was on the western margin of the

Pe” or
2onti

u
St
th

a
i
be n ntinent See pre- -Cambrian time also affected the western nite of

5 lantic coast to the ral Mountains.’

5 A comparison of the Atlantic Coast Cambrian series of America with
H) e Atlantic Coast series of Europe, as exhibited in Wales, shows a
= marked similarity between the sedimentation of the opposite sides of
_ the Atlantic. The basal Cambrian in South Wales, named the Caerfai
g oup, by Dr. Henry Hicks, consists of 1,570 feet of strata, as follows:
5 0 feet of conglomerates and greenish sandstones subjacent to a bed
f red shales and schists, 50 feet in thickness, above which 1,000 feet
Se niiteis sandstones occur. Dr. Hicks correlates the roofing alébes of
North Wales as found at Llanberris, Bethesda, and Penrhyn with this
ower division of the Cambrian, on stratigraphic evidence, as the few
Eoasila found are not sufficiently characteristic to correlate the two
: Series with each other or with the American Lower Cambrian. A com-
; arison of the sections with that of the southeastern coast of Newfound-

Ta: nd shows in each the presence of a basal conglomerate subjacent to a
“series of purple and green shales or slates. It is also to be noted that
the ‘Lower Cambrian of New Brunswick and eastern Massachusetts is
| .n ade up of shales of a somewhat similar character to those of the Caer-
fai group. It isa curious coincidence that the section of the Lower
| mbrian of North Wales is almost identical in the physical character
of its slates, including color and texture, to the Lower Cambrian roof-

tan g slate belt ol southern Vermont and eastern New York.

.

ey

fm ~
=

ee ae 10n the deposition of the Cambrian and Lower Silurian rocks. Quart. Jour. Geol. Soc., London, vol.
81, , 1875, Pl. 27, op. p. 558.
mee. Ba slostt, C.D.: The fauna of the Lower Cambrian or Olenellus zone. 10th Ann. Rep, U.S. Geol.
~ hanced PP: 568, 564.

‘those in Wales. In central Russia the Cambrian strata entirely dis- _
Zz appear and the Silurian (Ordovician) rests unconformably and directly —

e European continent, with a gradually diminishing force, from the.

Rte OF eOROPES 3TH

’

NE eh ae EE CAMBRIAN. pear pe ee x

- grits beneath 1,500 feet of gray, purple, and red rocks, above which 150

_ they belong practically to one province. In fact, there is no more dif

-vian group consists of 750 feet of slates and sandstones, and, with th 1@

drawn in the Tremadoc series between the upper and lower divisions

The Salva group of South Wales jatabete: of 150 feat. of yellowiat

feet of gray rocks occur, All three divisions are characterized by the
presence of the genus Paradoxides. The superior division of the Mene.

Solva formation, constitutes the Paradoxides zone corresponding to the
Middle Cambrian of the American section. This division is repre
sented in Massachusetts by the Paradoxides beds of Braintree, i in New
Brunswick by the Paradoxides shales of the St. John Basin, and in
Newfoundland by the Paradoxides shales of the Avalon Pein
The faunas of this division are largely identical on the opposite sides
of the Atlantic, and form the great connecting link that binds th
sections together and permits of almost positive correlation betweet
them. \o Se

The North American Upper Cambrian is represented in Wales ba
the Lingula flags and Lower Tremadoe series, formed of over 5,8 0
feet of biuish and black slates and flags with bands of gray flags E d
sandstones. The faunal and stratigraphic equivalent of this series has
been distinctly recognized in New Brunswick, on Cape. Breton Islan ;
and on the Avalon Peninsula of Newfoundland.

Most Euglish geologists have included the Tremadoe othe in th e
Cambrian ; but from an examination of the list of their contail ned fauna H
it appears to me that the line of demarcation between the Cambria
and Silurian, if- based upon the general facies of the fauna, should | be

The fauna of the lower division is essentially that of the Cambria
with a few genera and species more characteristic of the Lower Silue
ian (Ordovician), while the fauna of the upper division is largely of the
Lower Silurian (Ordovician) type, with a few forms of the Cambrian in
termingled with it. ES
he problem of the line of demarcation between the two groups it
England is essentially of the same character as that presented in Ne
vada, where there is no clearly drawn stratigraphic or faunal break it
the Pogonip series of limestones. ie
That there is a strongly marked resemblance between the Cambria
series of the Atlantic Coast Province of America and that of t
western Atlantic Coast Province of Wales there is no question.” an We
are able to compare the three main subdivisions and assume t ha

ference between the faunas and sediments on the opposite side of th
Atlantic than there is in different portions of the Appalachian Px
vince, and not as much as between different provinces on the “Nort
American Continent. ©

In explaining the strong similarity of the fone and sediments: 0
the Cambrian rocks of the opposite side of the Atlantic, Dr. Hemi

Hicks says: a

~
. — ie
. >

al - ey X ea
é ‘ iG

- oo ‘> a
ge VRS ET ee

Geo aA
wal

Loa possibly not far from the equator; and it is from here that the various

n to have migrated to the areas in which they were subsequently entombed.
igrations seem to have taken place towards the North American continent very
gf the same time as towards the pipe and the sea encroachments

it Rec to the east and northeast, so that the last lands wabrhotaed Would approaeh
each other : and oceupy the same region of the globe.

‘The Seandinavian Cambrian series is not over 200 feet in ihinkueia
bea! * represents the entire British series.? It is divisible into the Lower
Cambrian or Olevellus zone, the Middle Cambrian or Paradoxides 2OnE
and the Upper Cambrian or Olenus zone.

On the opposite side of the Baltic, in eastern Estoria, the Lower
Ca nbrian zone alone is recognized by the presence of its characteristic
“fauna. The Middle and Upper Cambrian faunas probably existed in
eth is region, but they have not as yet been discovered.

e rat may represent the Lower Cambrian. Qhe Upper Cambrian, if it

las not been removed by pre-Silurian ero sion, does not appear to have

“none!
- The Gaibbrian rocks of the north of France are correlated with the
iu ambrian of St. David’s, Wales, by authors, but they are not sufficiently
| well defined by faunas to compare them with American formations. In
th he provinee of Hérault, in the south of France, the presence of Para-
~ doxides correlates the Sock with the Cambrian a Bohemia.*
¥ * On the island of Sardinia there is a mixture of Middle and Lower
~ Camb rian faunas, which may arise from the confused state of the strata,
pe itis not impossible tbat the faunas are really mingled in the same
eds. In the absence of more definite data it is not practicable to com-
re _ pare them with the American sections.

Ls

' The contrast between the American and European Cambrian, with

4

% the exception of the sections of Bohemia and Sardinia, are not as great
= those between the Atlantic Coast Province and the Appalachian
AP” rovince, or as between the Atlantic Coast and Rocky Mountain Prov--

%

a 10n the deposition of the Cambrian and Lower Silurianrocks. Quart. Jour. Geol. Soc., London, vol.
_ > 81, 1875, p. 555.
ay 3808 Prof. Charles Lapworth’s comparative table of the Cambrian rocks of Britain and Scandinavia.
me fs pgserinls for the Correlation of the Lower Paleozoic Rocks of Britain and Scandinavia.” Geol.
C , new series, dec. 11, vol. 8, 1881, pp. 320, 321.
ihe. J: E. Marr correlates the basal beds of Barrande’s Ktage D (d 1a) in which Lingula feistmanteli
occurs in abundance, witb the Lingula flags of Britain. Quart. Jour. Geol. Soc., London, vol. 36, 1880, -
= ; ;

ae. Jules: Note sur la présence de la Faune primordiale (Paradoxidien) dans les environs
e Ferrale-les- Montagnes. Bull. Soc. ee: France, 3¢ sér., vol. 16, 1888, pp. 282-285.

ae . xo , atte : 4 , =e iy cz
ae ee Ay pay ANG aetaere aoe

aga the Susie eae of life seems to have been somewhere towards the ;

“Beneath the Paradoxides zone of central Bohemia there is a consid--
erable thickness of Shales, grits, schists, conglomerates, and quartzites —

. een clearly differentiated from the Middle Ganiirinn or Paradoxides |

ee satay gia eon, said le ee Se Ps ooo ORS
Re JO : ML ; wr - x & rs : a a t Fg Ni . { tot ; sea? 9 is . ves
, , \ ‘ oe , § -
3876 Bs 6, ‘THE CAMBRIAN, | ke ING ES eR bo ee
. rs = f 5 Jee AY Ake # ~% 5 ie

- Paradoxides fauna, but not in other details. : ;

+r

“western Europe are on the eastern side. The Bohemian area and t

(Ordovician). The English geologists have included the Upper Tre- 1

Cambrian, because a local stratigraphic break occurs at their summit és

‘western Scotland may be referred to the Lower Cambrian. Prof. Ar: |

_* * * The denudation must have been considerable even in early ‘Silurian.

~ -

inces.. _ In point of. fact the Aulonge: Coast Province of Aimertotal
practically a portion of the Atlantic Province of which the sections of

represented by the deposits on the island of Sardinia partake, in party
of the character of the Atlantic Basin deposits, in the presence of the

The essential difference between the English and the American clas-
sification is in drawing the line between the Cambrian and Silurian’

madoc slates, with their strongly marked Ordovician fauna, in the

and between it and the subjacent Arenig series. By the definition
adopted in this paper for distinguishing the great geologic groups, the
Upper Tremadoc slates, with their fauna, would be included in the Si-
lurian (Ordovician), and the line of delimitation between the Cambrian
and the Silurian (Ordovician) be drawn at the base of the upper Tre-
madoc slates, thus referring the Lower Tremadoe and the Lingula flag”
series to the Upper Cambrian, and the Upper Tremadoc to the base. 7
Silurian (Ordovician).

In conclusion: (a) The relations between the Gambrivs rocks of the
eastern or Atlantic coast,of North America and those of Wales are of a
genetic character, and point to their having been deposited in thesame time
interval; (b) the Scandinavian Cambrian represents the same interval, |
but with a greatly diminished bulk of sediments; (c) the French and.
Spanish sections are too incomplete for close comparison, althoug :
representing the coast of Wales series; (d) the Bohemian and Sardinian
areas point to local conditions that may have affected their connequyaa
with the typical Atlantic Basin sediments and faunas, Be

SCOTLAND. Aha = <4

The occurrence of Cambrian rocks in Scotland has not yet been fully

proved, but it is quite probable that the Torridon sandstones of north

chibald Geikie, in summing up the notice of the Cambrian rocks. in ;
Scotland in his Text Book of Geology, Says: <2 a

In the northwest of Scotland a mass of reddish brown and chaoatnseaelened sand- ‘
stone and conglomerate (at least 4,000 feet thick in the Loch Torridon district) lies.
unconformably upon the Archean gneiss in nearly horizontal or gently inclined b

times, for the sandstones are unconformably overlaid by quartzites and limestones ¥.
containing Lower Silurian fossils, and these younger strata even in the same distrie’ t
rest directly on the Archean gneiss. * * * No trace of organic remains of any
kind has been found in the red sandstones themselves, unless certain track-like im #3
pressions, observed on the west side of Loch Maree, can be regarded as having bem!

imprinted by crustacea or other organisms. A es ;

1 Text Book of Geology, 1885, p. 653.

.

>. ‘he supposed Conteuatunays of the Welch Cambrian series in the
., “sol southeast of Ireland is described by Prof. Geikie as follows:

—_ Btn Sauna of Ireland, masses of purplish, red, and green shales, slates, grits,
‘Ay -quartzites, and schists occupy a considerable area and attain a depth of 14,000 feet
e, without revealing their base, while their top is covered by unconformable formations
td Q ower Silurian and Lower Carboniferous). They have yielded Oldhamia, also numer-
ous burrows and trails of annelides (Histioderma hibernicum, Arenicolites didymus, A.

ie _ sparsus, Haughtonia pecila.) No Upper Cambrian forms have been met with in the
Irish rocks, which are therefore placed with the Lower Cambrian, the unconforma-
e bility at their top being regarded as equivalent to the interval sean for the depo-
sition of the intervening formations up to the time of the Llandeilo eb a as in the

x hee of Scotland.!
: as

zx very full description of the Cambrian rocks of Ireland, especially
as they occur at Bray Head, Wicklow, is given by Prof. William Hellier
Baily i in 1865. A Sesottinitintic section accompanies the paper, and the
author also describes the supposed organic remains that have been
found i in the rocks.” )

~~

f
ae

by
7%

CHINA.

enix arnicdes of the Cambrian rocks of China results from the
Be avestigations of Baron Richthofen in the province of Liau-tung in north-
FE eastern, China, near the Corean frontier. He found a series of lime-
a. stone containing the “Primordial” fauna in the sections of Sai-maki
and Tai-tsze ho.2 The limestones are superjacent to a series of sand-
os ‘stones and quartzites that correspond in stratigraphic position to the
s Lower Cambrian of North America.
i a The collections of fossils were studied by Dr. Wilhelm Dames, who
3 came to the conclusion that two horizons were represented—the An-
-drarum limestone or Paradoxides horizon of Sweden, and the Quebec
3 horizon of North America.* At the time Dr. Dames wrote Dikeloceph-
alus gothicus and D. quadriceps, which he referred to the genus Dor-
“opyge, were cited as from the Quebec group; and it was on the com-
AS parison between the Doropyge richthofeni and these two species that he
Bs considered that the Quebec horizon was represented. The two species
~ tentioned are now referred to the genus Olenoides of the Middle Cam-
_ brian fauna, which is not known to occur in the Upper Cambrian or in

; 4

sae the: species illustrated by Dr. Dames leads me to think that the Middle
chia, fauna only is present, although it is not impossible that
~ some Upper Cambrian species may have been collected. The sections
of Baron Richthofen, however, indicate a considerable thickness of con-

ms cs 1Text Book of Geology, 1885, p. 654.
2 The Cambrian rocks of the British Islands, with especial reference to the occurrence of this forma-
x ~ tion and its fossils in Ireland. Geological Magazine, vol. 2, 1865, pp. 385-400.

Be (das nordliche China) fig. 21, p. 94; fig. 29, p. 101, 1882.
RS oe Trilobiten von Liau-tung. China; by F.F. von Richthofen, vol. 4, 1883, p. 33.

eaters Pie I avd Cee pet ORS Ne te Sy Be fae RRS eG Ae f ye. Tae eee
eh Sere ie Gee 5 * a2 a ern ae
ee IRELAND—CHINA. iS eee 377
; r .
IRELAND.

the Caleiferous-Chazy fauna corresponding to the Quebec. A study of.

Ss %Richthofen, ¥. F. von: China. Ergebnisse eigener Reisen und darauf gegrundeter Studien. Vol.2

NEN, Sie ie Green fear ee fae Sue Ut bale te aes eh Pa ME SS og
par aa, edie Mir te ee de hg a we ea Ae Pet Wie’ a te

- “eh eS he . St a ee = Pay. wd Aer :

| bin Bras bate a bos EE ‘THE CAMBRIAN. es Oe ye

crete in which the Ui ppek Cambrian fauna may possibly be diccoaaele :
The geologic section is to be compared to that of the Rocky Mountain — ei
Province, and the presence of the same peculiar Middle Cambrian — a
_ fauna, unmarked by the aonas Parado xides, also strengthens the com- » a
“parison. | *

> 1

INDIA.

In a note on the discovery of trilobites by Dr. H. Warth. in the:
Neobolus beds of the Salt Range, by Mr. Will King, director of the _
Geological Survey of India,' it is stated that the trilobites were dis: a
covered in the Neobolus beds of the Salt Range. The stratigraphic —
succession, from the summit downward, beneath the Carboniferous — )
limestone, is as follows: ? ° ; . |

7. Red shaly zone (Salt-pseudomorph zone).

Magnesian sandstone group.< 6. Magnesian sandstone,
5. Dark shaly zone (Neobolus beds).

4, Upper purple sandstone (purple sandstone).
3. Rock salt and red gypsum group. <3
2. Gray gypsum group. : SS

Purple sandstone group.
1. Lower purple sandstone.

There had been previously discovered in the Neobolus beds by Dem
Warth and Dr. Waagen a number of brachiopods, which were described
by Dr. Waagen as follows: Discinolepis granulata (p. 750), 8 chicopholig = :
rugosa (p. 753), Neobolus warthi (p. 758), N. wynnei (p. 759), Davidsonella —
linguloides (p. 764), D. squama (p. 766), Lingula kiwrensis (p. 768) ana! *
—warthi (p. 769).3 :

It is stated that the trilobites were sent to Dr. Waasen: who identi A
one of the two determinable species as a Conocephalites, very nearh, 4
related to Conocephalites formosus Hartt, from the St. John- fib! nd
the other as probably an Olenus. ; e.

‘The beds in which such forms occur can not be anything but Cambrian, and they $
must probably be classed as referable to the upper region of the Lower C mubrians sy

In the table the probable equivalent elsewhere of this formation is
the Sinic formation of Richthofen, in China.° a

4

AUSTRALIA.

- The Cambrian rocks of Australia appear to be coufined: to the south 7s
eastern portion of South Australia and the northern portion of Tas-
mania. In the ‘Papers and Proceedings of the Roy al Society of
Tasmania for 1882, ” Mr. R. era jes devon bee a Age ot. Con oo

1 Records of the Geological Survey of India, vol. 22, 1889, pp. 153-157,
2 Op. cit., p. 157. ~~ s

3 Memoirs of Geol. Surv., India. Palzeontologia Indica, ser. xiii, vol. 1, 1887, pp. babs Py ay
4Records of the Geological Survey of India, vol. 22, 1889, p. 154. - ; a
SOp. cit.,p.157. ae: “a

oe «,. a A aS. a tle - -. » Blow” , »
wlieg " Le ae te Me eet . = aj “
: > 7 we A

mee mee SOUTH AMERICA. Fp 879

<a

a Medixen.’
---‘The trilobites and the -gasteropods are correlated with the Upper
ae - Cambrian fauna of America and Great Britain, to the Potsdam sand-
z % ‘stone in America and the Lingula flags of Wales.
2 In 1884 Dr. Henry Woodward described some trilobites from the
s -Parara limestone of the Yorke Peninsula, South Australia, Conocepha-
lites australis and Dolichometopus tatei.2. He concludes that the trilo-
- ites are clearly of Lower Silurian age, being equivalent to the Swedish,
Bohemian, Tasmanian, and North American beds with similar fossils,
A recent paper by Mr. R. Etheridge, jr., on some Australian species
33 _ of the family Archzeoc yathine describes the presence of several species
_ of that family in association with trilobitic remains at Ardrassan, Yorke
Peninsula, South Australia. The species described are Ethmophyllum
__ hindei, Protopharetra ? scoulari and Coscinocyathus tatei3 —
The strata containing tbe fossils are correlated with the Potsdam
horizon sandstone of America or the Lingula flags of Wales. From
$ ans the stratigraphic position of the American forms of Ethmophyllum
and Coscinocyathus it is quite probable that the Australian species
~ belon g to the Lower Cambrian fauna and not to the _Upper, as identi-
- fied by Mr. Etheridge.

SOUTH AMERICA,

In 1876 Dr. Emanuel Kayser deseribed a small collection of Primor-

ae dial fossils made in the northern portion of the Argentine Republic, in | :

_ the provinces of Salta and Jujuy, by Prof. Lorentz and Dr. Hyeroni-

mus, of Cordova. The fossils occur in a micaceous sandstone, and in- —
4

elude the genera Lingula, Obolus, Orthis, Hyolithes, Arionellus, Agnos-

: Sof Europe and North America, and concludes that it belongs to the upper
-. zone of the Primordial. He calls attention to the fact that the genus

tus and Olenus.t Dr. Kayser compares the fauna with that of the north |

: Paradoxides is wanting and that Olenus appears in great numbers, —
“This fact seems to indicate that our fauna belongs to the upper Pri- ~

mordial zone or the Olenus stage.”

A glance at Pl. 1, of Dr. Kayser’s memoir proves that he is correct in

Aon the reference and that the fauna is of the type of the Upper Cambrian.
From the geographical position and character of the fauna it is quite

onl

Ptncitiable that Cambrian formations will be found on the eastern slope

~ of the Andes, as well as the Cordillera of Central America and Mexico,
-if not concealed by later deposits.

"3 iat

4 ay 1 Paper s and Proc. Royal Soc. Tasmania for 1882, 1883, pp. 151-158.

- _— #Note. on the remains of trilobites from South Australia. Geol. Mag., new series, dec. m, ee
1884, pp. 342-344.

~~ 80n some Australian species of the family Archeocyathing. Trans. Roy. Soc. South Australia,
__ vol. 13, 1890, pp. 10-22, Pls. 1 and 111.

Bs fe 4 Beitrage zur Geologie und Palaeontologie der Argentinischen Republik; Palaeontologische
_ Theil.; von Dr. Emanuel Kayser, Cassel, 1876, pp. 28.
om “Op. 5 rel 29. ‘

te

-

F Ars d's ie Se picts tees Be. bi x oes iat re ae ee A bag adh y on: rsa ee aes sities ed S ’

~~ and the pre-Cambrian rocks of Trinity and St. Mary’s Bay, as ee

_ of the relations of the Olenellus bearing strata to the subjacent and

*

i ‘aS , ie a Sah Ne ete
- - - ae s » bene
S25 YES ; Ey =X ple uf ut foal
. ‘ i : 5 a rs =~ AY ix inet
eA Se | nS eo Si ne ra

= k eS ; wt see Z Se ay a =e on “= OT ee =

Rees a
on de

2 see = ‘ > Py +3
“ L

OHAPTRR(V. 3. 2S ee

PROBLEMS FOR INVESTIGATION AND SETTLEMENT. - __

‘

I.—Local problems within the subdivision of each province. ‘ ‘ A
II.—Problems affecting our Knowledge of the Cambrian group as a whole or in large parts, .

IIl.—Probiems of nomenclature and classification. -

“LOCAL wapuriaire:

There are many local problems that are not mentioned in the follow- —
ing notes. With the settlement of the more important questions they of
will assume prominence, and some of them may prove to be equal to —
if not of more import than those now suggested for investigation. |

Newfoundland.—The prominent questions are:

(1) The determination of the relation of the Cambrian rocks of St.
Mary’s and Trinity Bays to the basal conglomerate in the Manuels 3
Brook section, to ascertain if a series of Cambrian strata occurs between —
the lowest recognized Cambrian on Conception Bay and Manuel’s Brook _

by the Newfoundland geologists. If such a series be found its fauna —
should be carefully collected and studied with reference & its being
basal Cambrian or pre-Cambrian. «ae
(2) The discovery of an unbroken stratigraphic section to prove the q
assumed relations of the Paradoxides fauna to the Upper Cambrian — 4
fauna. This will probably be found in the vicinity of or on the shores x
of the peninsula west of St. Mary’s Bay and the shores of Wasi
‘Bay. : :
(3) The determination on the west and northwest sides of the ‘sanded .

superjacent beds and the character of the section from its base to the — :
limestone carrying the Calciferous fauna of the Silurian (Ordovician). .

(4) The study of the geographic distribution and detailed sections of
the strata on the southwestern and northeastern coasts. ~

(5) The relations of the Cambrian strata to the superjacent beds of.
_ the Silurian (Ordovician) wherever they can be found in the same sec.
tion. A
Nova Scotia.—The fae question in Nova Scotia, as in Maras ‘
and New Hampshire, is the determination of the geological age of the ;
slates referred provisionally to the Cambrian. After this come the —
local details of the sedimentation and paleontology of the Cambrian 4 .
terrane. Until the first is decided very little except conjecture can be —
used i in the correlation of the slates with the Cambrian < ‘Or other ie i 4

I ? at

>. oer eee
* as. ¥ a a
i a FY on AY

ao hae cP PY Lee Ter rye? nl) edt tal oe ‘ ‘ a. ‘ aoe ac 3 ok es
bee w= . % wt Yori | 2 A bee : a a> ag ® . -e. 7 _ ; .
7 ‘ “ \, > tn

pa
~

: By I New B Bruntoict. <taroaek the efforts of Mr. G. F. Matthew many of

i agent solved. More information is needed for—

(1) The clearer identification of the Lower Cambrian or Olenellus
a Zone and its exact stratigraphic relations to the Paradoxides zone.

: 2 (2) A clearer determination of the Upper Cambrian fauna and its re-
— lations to the Paradoxides zone.

4 (3) It is desirable that more data should be obtained upon the zo-
paee relations of the different faunas to each other.

Maine and New Hampshire. —The problem presented in Maine and
ie Hampshire i is essentially of the same character as that presented
in Nova Scotia. It is the determination of the presence of rocks of
_ Cambrian age by paleontologic evidence. Until this is done the other
ot problems of stratigraphic succession and geographic distribution of the
e. Strata and faunas can not be considered.
~ Eastern Massachusetts.—In eastern Massachusetts it is desirable to

-ascertain—

(1) The stratigraphic relations of the strata carrying the Olenellus”

“a enue and Paradoxides fauna and decide whether the Upper Cambrian
q a is represented in the region. |

(2) To obtain more paleontologic data in order to correlate tbe vari-

a & “ous outcrops that have been referred to the Lower and Middle Cambrian

ee in different portions of the Boston Basin and to the south-southwest
2 - - toward the Rhode Island line.

_ (8) To identify and map the Cambrian rocks in detail.

~ New York.—In New York it is desirable to ascertain—

(1) The exact relation of the strata carrying the Olenellus fauna to
hoes carrying the Upper Cambrian or Potsdam fauna about the Adi-
_ rondacks.

», (2) The stratigraphic succession and thickness of the strata carrying

3 ne > the Olenellus fauna in Rensselaer and Washington Counties, and |

whether the Middle and Upper Cambrian can be recognized either by
Ss we faunal or lithologic characters.

, (3) The geographic distribution of the Cambrian rocks in the Hud-

5 ‘son. Valley south of Rensselaer County.
Adirondack subprovince.—The most important aaoblom: in connection
with this subprovince is the tracing of the transition from the sand-
3 stone of the Potsdam about the Adirondacks to the off-shore deposit
3 a represented by the shales and slates now found beneath the limestone

Ee the marble belt of western Vermont and eastern New York. More ~
_ extensive collections of fossils are also desirable for the purpose of in- ~

q Se sitting closer correlations between the faunal zones of the typical
Potsdam section of the Adirondacks with that of the correlated sand-
_ stone of the Mississippi Valley and elsewhere.

Vermont. —In Vermont the problems presented for study in connec-

; problems relating to the Cambrian system in New Brunswick have —

Bae with the Cambrian rocks are somewhat of the same type as those

E Cs ‘ PROBLEMS FOR INVESTIGATION. 381 “

ig

a , = “+ re! Si eet Ce oe oe mt oe re > ae
Me a Pe pe ; fet ate m ee
4 ¥ ~ ~~ ™ == x al ine > AE ant ae as x TA a, * Lin
; rote STS). Shy ze
882. ny _ THE ‘CAMBRIAN. - Reg Bers

of Ne ew York: “They differ i in on northern sila owing ir tothe vary: =
ing character of the sediment. Some of the questions are— =
(1) The relation of the lower band of limestone (“4 Red ‘sandrock 4
bearing the Olenellus fauna, to subjacent rocks. a
(2) The relation of the shore-deposits, forming the ‘ Granular Quartz” 7
_ on the western slope of the Green Mountains, to the off- -shore deposits, _ 4
forming the limestones (“ Red Sandrock”) and shales (Georgia, ete.) a
carrying the Lower and Upper Cambrian faunas, in northern Vermont.
(3) The change in character of the sedimentation of the Cambrian .
rocks from the northern to the southern part of the State and their F
- transition into the shale and slate series of New York. 4
(4) The determination of the extent of the range of the Cambrian —
fauna in the limestones of the “ marble belt” in sonthern Vermont and —
the relations of these beds to the subjacent Cambrian strata on the — “a
western side of the * marble belt.” The latter involves the question
_ of the relation of the slates and shales carrying the Olenellus fauna and, —
in part, the base of what may be a portion of the Middle Cambri i
fauna to the limestones. The working out of the complicated struc:
tural geology and the identification and mapping of all the formations —
will be required in the solution of these problems. Ge
(5) The determination of the absence or presence of paleontologic
data sufficient to differentiate the three primary divisions of the Cam. “
brian group. >a
(6) The detailed geographic distribution of the formations ‘referred
to the Cambrian throughout the State. " q
Canadian extension.—The Cambrian group on ne line of the Cana-— f
dian extension north of Vermont, in the vicinity of Quebec and down —
the St. Lawrence River, requires detailed study in all its parts, both to
determine the stratigraphic suecession and character of the beds and —
the relation of the strata to the subjacent and superjacent series. One- =
of the important problems presented is the determination of the origin —
of the limestone bowlders in the Point Levis conglomerate that carryey
the Upper Cambrian fauna, and those of the Sillery shale that carry ©
the Lower Cambrian or Olenellus fauna. In fact, the entire Cambrian» SF
group of this portion of Canada requires full investigation.
New Jersey.—In New Jersey it is desirable to ascertain :
(1) The relation of the quartzite that has been referred to the Pots: E
- dam, to the subjacent Green Pond Mountain rocks. ‘ a
(2) The representatives in New SSLOEY of the Pennsylvania Primal
‘slates of Prof. Rogers. s ‘a
Pennsylwania.—Iin the State of Baretta cs attention should be
given: 2 ‘
(1) To determining, by paleontological evidence, the exact age of thon
quartzite which has been referred to the Potsdam sandstone - by. ‘aia
authors. | e
(2) To a careful study of the upper Primal ‘alias for the purpose of
determining the line of demarcation between the Saeco and Blk u- <

a

* ° ee
Pe sey

4 ocieiadle sendokoa. as "sie. Se aesakis series is unbroken
i and there is a gradual gradation between the schists or slates and the
Peer by the intercalation of calcareous beds in the shales until the
latter predominate and form the limestone series. ‘Chis investigation
an probably be best carried on in York and Adams Counties and the
western portion of Lancaster County.
~ careful investigation all along the line of contact of the two terranes.
3 ce (4) Another problem that requires investigation is whether the Pri-
mal slates and schists graduate into limestones to the east and north-
_ east of Lancaster County, or whether there is a line of uncomformity,
“by non: deposition, between the quartzite and limestone in Chester,
. _ Berks, Bueks, Lehigh, and Northampton Counties. In other words,
% whether the portion of the Cambrian section as found in York and
Be _ Adams Counties is absent in the counties to the northeast, or if it be
3 _ represented by the lower portion of the limestone series.
BS _ Virginia.—The knowledge of the stratigraphic position of the rocks

_ condition than that of Pennsylvania, It is desirable, however, that
attention be given to: ;

a a (i) The changes in the character of the sedimentation from the Ten-
- nessee line north to the Potomac, and also the changes in the character
| of the sediment between the shore deposits of sand and conglomerate

and the off-shore deposits of shale and calcareous matter.

rm! oF Po Sie “Hz a ay mes Ab on en ie, ¥

PROBLEMS ‘FOR INVESTIGATION. Siler! | oa

(3) The relation of the quartzite to the subjacent rocks also requires

referred to the Cambrian, in Virginia, is in a much more satisfactory.

- - 2) The -paleontologic evidence of the geologic age of the stratare- —

a — to the Cambrian, is very defective, and investigation in this line
_mioala be made throughout the State. ;

North Carolina.—The problems to be considered in North Carolina

RT). The section along the French Broad, so as to determine the age

a of the strata and, if Cambrian, ascertain the stratigraphic position of

: the limestones, shales, ssndstonss, and quartzite to each other and to

oe sections of eastern Tennessee.

ay * (2) About the same problem is presented in the rocks on the line of
z ‘the Hiwassee section, in the southwestern portion of the State.
__ -Fennessee.—The questions requiring investigation in Tennessee are:
(1) The stratigraphic relations of the Chilhowee formation to the
€ ae sandstone and Shale series.
be (2) The relations of the eastern shore deposits to the off-shore deposits
3 & _ westward of the pre-Cambrian rocks.

BPS. =e The collection and the study of the faunas of the Chilhowee and
a Knox-shale formations.
i (4) we geographic distribution of the strata and the vertical range

S xe

Beergia ia Alabama. —The entire Cambrian section of Georgia and
l bama needs to be worked out stratigraphically, especially the rela-

4 ’ . “
__ a “ ‘ 4
Ena’, %
ae : >

~ varied, and should be studied in connection with that of the Cambria un

a eR hg es eR Ree Se Sipe SN Sh ee
J St . ba ee - e i, e rae Pee

tc Mae cata Pee : THE CAMBRIAN. oe ae (oor

a. ' a os

tion of the Coosa Valley shales to the gharieiton referent ‘the ol pil-
howee formation of Tennessee. The fauna of the shales is large | ang

section of Tennessee and New York.

Utah and Nevada.—The problems awaiting solution in bi study ¢ of
the Cambrian rocks of Nevada and Utah are of an unusually interestir g
character. Those that suggest themselves are:

(1) The study of the basal beds of the Ca mbrian, and the possible
tension of the Olenellus fauna down into the quanbaea series bene
what is now recognized as the Olenellus zone. From ail that is known
to me of the rocks in Nevada and Utah, I think that in western centra
Nevada the best opportunity will be found for the discovery of da
faunas preceding the present recognized base of the Cambrian. Dur-
ing later Algonkian time there appears to have been a great accumu:
lation of arenaceous and siliceous sediments along the line of the Wa-
satch and extending west ward into central Nevada. In western N evada
they are more shaly and calcareous, and it,is possible that the condi- |
tions under which they were deposited were more favorable for the
presence and preservation of the life of that period.

(2) The careful and detailed study of the great Cambrian section” ‘of.
central Nevada for the purpose of determining the full sequence of life
throughout. Our present knowledge of it is very incomplete, and there
are many gaps that ca n probably be filled in by detailed work and the
careful collection of the fauna in connection with iy study of; strat:
graphy and sedimentation. 24

(3) The study of the sections from the Wasatch westward to western —
Nevada for the purpose of determining the change i sedimentation and
life from east. to west. a

(4) Another important subject of investigation is the transition be:
tween the Upper Cambrian and Ordovician faunas. This has been par- |
tially worked out in the Eureka district section, but there still remains: a
much to be learned by careful detailed Teast of the sediments and 4
faunas in the field. a

(8) One of the unsolved problems of Utah is the abies of the geo-
logical age of the quartzite beneath the Carboniferous limestone sur-
rounding the main quartzite series of the Uinta Mountains. It is
probable that there is a series of Cambrian rocks beneath the limestone -
and above the quartzite as in the Big Cottonwood Cain section of the
- Wasatch Range; but it will remain an open question until pa: ‘conto
logic evidence is obtained. 7

Colorado.—Investigation in Colorado should be directed toward dis
covering fossils in the strata referred to the Upper Cambrian zone, and
to verifying the exact stratigraphic position of the beds carrying —
Dikelocephalus at Quandary Peak.
Rocky Mountains.—In the eastern district of the eee Mountain
Province it is “desirable that close study should be made of the various

a
Z

k

~

a

“PROBLEMS: ‘FOR INVESTIGATION. 385

’ * Y AA "~,' _ {= = -—» «
i+ > “ _* . 7, . ‘4
nas a . i-s P 7 <
Sia < 2 ik
7 o.~ - . .
~ ah . ‘ ‘
+ 4.

3 ‘the ie purpose of detecting the presence and character of the fauna as
a me eans of correlating the strata with those of the Black Hills and the

Gallatin River section needs special investigation in order to cor-
‘it with the sections of Nevada. Reference to what is roquny in
Nevada, and Colorado has already been made. :

e lower sandstone of the Cambrian section in the Grand Caiion area,

be determined.

Minnesota surveys our knowledge of the Upper Cambrian sandstone is
w
a tained’ in relation to the distribution of the fauna in the section and
gto ascertain whether the Middle Cambrian fauna accompanied the in-
; rasion of the sea that deposited the lowest beds of the terrane.

| ‘Superior it is still necessary to obtain paleontologic evidence to enable

be nivalent of the fossiliferous sandstone of the central area of Wiscon-
oe It is also desirable to trace the continuation of the recognized.
fossiliferons Upper Cambrian sandstone directly west of Green Bay,
Wisconsin, with that occurring on the south shore of Lake Superior.
pr he 2 definite Settlement of these two problems will remove what has long
be xen the source of contention among geologists. .

& Missouri.—It i is desirable that the exact line of demarcation petuenl
2 the Upper Cambrian and Silurian (Ordovician) zones should be deter-
‘ei 1 nined and more positive paleontologic data be obtained of the relative
_ Stratigraphic position of the beds with those of other areas that are
now referred to the Cambrian.

_ Texas.—The information in relation to the Cambrian area of central
Texas, in Llano County, i is sufficient for most geologic purposes, although
: more detailed information as to the horizontal distribution of the fauna
am and the presence or absence of the Middle Cambrian fauna is desirable.
= principal question, however, is the investigation of the supposed
Cambrian in the vicinity of El Paso and the southwestern portion of

a7 Meese ~, ; }
a. AFFECTING OUR KNOWLEDGE OF THE CAMBRIAN GROUP

AS A WHOLE OR IN LARGE PARTS.

tay S
eS

~

strata as shown by outcrops in North America, Pl. 1, reveals at once

th
as ee

s of sediments that are largely covered, over great areas, by later
~ Bull, 8125 :

r "Mississippi Valley. On the western side, in southeastern Idaho, —

ts |
Arizona. —lIt is desirable that larger collections should be made from
3 d that the geographic distribution of the Cambrian in western Arizona —
we Mississippi Valley.—Through the work of the Wisconsin and

usually complete. It is desirable that more information should be —

4 “To determine the age of the sandstones on the south shore of Lake ©

2 the geologist to state positively that the sandstones are the geologic —

Blancs at the map delineating the distribution of the Cambrian

» fact that we are dealing almost entirely with a marginal or coast

YS hae PO ne nS ee Ns OE ne Pe ee, Seah Ga tare Tae fe ne ile ag
~~ ae ‘. - we “ b Sty ‘ Foe ' Ly . as
: : 7 .. . “ KW, - SS CR

oer ps a ‘3 ae ie
oN virdt Yau c ; F~, vos SEERA Gate sy >)
386 ey ener THE ‘CAMBRIAN, bee att
; Vrs bh eae Se

deposits. It i is only here aa there that a deep-seated Hatachawee has”
brought up the sediment that accumulated at some distance from. the*
Shore line. In Vermont and Nevada, especially in the latter, the
calcareous sediments forming the limestone have been brought. to the
surface. In the great interior area of Wisconsin, Missouri, Texas, and
the eastern front of the Rocky Mountains and the northern line —
- between Canada and New York eta is known of the sy water
deposits, if any such existed. :

We know something of the sediments that negaiilagen along’ thei |
western shore line of the Appalachian protaxis; but what was de-
posited over the area of which Ohio, Indiana, Kentucky, Tennessee, —
northwestern Alabama, Mississippi, northern Texas, Indian Tornor ea
_ Kansas, and Nebraska forms a part we know nothing.

From the fact that in Texas, Missouri, the Upper Mississippi Valley,
along the eastern front of the Rocky Miugsions and in New York and
Canada west of the Adirondacks the deposits are such as would F-
accumulate in a shallow sea not far distant from the shore line it has |
been assumed that the Cambrian ocean of this great area was rela-—
tively shallow. I think that during Lower and Middle Cambrian times —
_ the entire interior continental area was above the sea level. These —
opinions are based on the character of the deposits and the absence of
the sediments of the Lower and Middle Cambrian. The great problem ~
in this connection, however, is to determine how far the pre-Cambrian _
continent extended to the south and east and what its relations were
to the offshore ridges of the eastern and western margins, along which
_ we now find deposits of Lower and Middle Cambrian age. ;

A careful study of the sections in Pennsylvania, Virginia, Tennessee,
Georgia, and Alabama may throw some light upon the question on
the southeastern side. Over the remaining portions of the great cen-
tral area no natural outcrops are known, and there seems to be no way .
of obtaining information except by very deep borings. a

The question of the relations of the Middle Cambrian fauna of the
Atlantic Coast Province to that of the Appalachian and Rocky Moun-
tain Provinces is one that can be settled only by a close and careful
study of the faunas, based on large collections methodically made
throughout the entire areas of the three provinces. That the Middle |
Cambrian or Paradoxides fauna of the Atlantic Coast Province is rep-
resented by a very different fauna in the Rocky Mountain Provineg
there is not, I think, any question. It is also well proved that the
latter fauna is present to a less extent in the Appalachian Province. —

Throughout the Rocky Mountain Province, except in British Colur a
bia, the Olenellus or Lower Cambrian fauna is confined to a very nar-
row zone, while in Vermont it ranges through 1 ,000 feet of limestone =
and up into the superjacent shales. In New York it has aran Sees
a great thickness of shales, slates, interbedded limestones, and sand-
stones; ; and one of the problems PeaDS inveengons is the downward 1

Rhee eo SY spe ee Mears Sb ere 7

a

eath the now known Olenellus horizon of the western Rocky Moun-
in Province. The lower series of slates and quartzites have been
ter atively: referred to the Algonkian, but it is quite probable that
ag hey will be found to carry the Olenellus fauna to a considerable depth,
1d a pre- -Olenellus fauna may yet be discovered.
E a problem of the downward extension of the Cambrian faunas also
re requires investigation in the Appalachian Province, especially in the
* Bs southern portion—in Tennessee, Georgia, and Alabama. The basal
~ limit of the Cambrian is now drawn at the Olenellus zone, but in the
3 absence of any subjacent fauna there still remain the problems of the

_: downward extension of the Cambrian fauna and of the existence of a
_ re- -Cambrian fauna that may have lived in the Appalachian seas.

considerable area and involves conditions of sedimentation unknown

cin. and mode of transportation of the bowlders of the limestone con-
x ~ glomerates that carry in the lower zone, the Lower Cambrian, and in the
a of the St. Lawrence River from Quebec to Gaspé.

sa One of the problems partially solved, and one that still requires in-
a vestigation, is the relation of the pre- ‘Cainbrisn topography to the sedi-
ments deposited upon it, to determine the source of sediments and the
habitat of the faunas.
a es _ Along the Atlantic coast the presence of the pre-Cambrian shore line
ee with a varied coast topography is clearly distinguishable, and it is evi-
= dent that the Cambrian strata now occupy the same relative position to
Pa pre-Cambrian as the sediments did when they were deposited. The
= - Same i is true of the shore-line deposits along the western margin of the
; Appalachian, pre-Cambrian protaxis, and the sediments about the Adi-
BY - rondack area. Between the Adirondacks and the Green Mountains a
ie 3 _ great thickness of Cambrian rocks appears to have been deposited in a
- deep, relatively narrow sea; but what the conditions were to the west-
es _ward of the long line of the eastern boundary of the Appalachian Prov-
ince is one of the questions requiring solution. The same is true of the
es of the sediments now exposed in the great uplifts of
_ central Nevada and British Columbia.
: es. - The questions arising from the study and comparison of the various
provinces all require a more thorough investigation of the sections of
e he western Rocky Mountain, Appalachian and Atlantic Coast Prov-
oi inces. They bear upon the nomenclature and classification to be adopted
. aa 3 for the Cambrian group; and not until we havea more thorough knowl-
#4 edge of the sections of northern Vermont, New York, Tennesse, British
aia and Nevada can the classification be considered more i a

_ provisional one.

fe PROBLEMS FOR INVESTIGATION. <s 387

_ A local question of interest may be here introduced, as it affects a

elsewhere i in the Cambrian. It is the question of the place of deriva- _

_ upper zone the Upper Cambrian fauna found along the southern shore.

a

sion. of this fauna i in the series of aise: slates, and sandstones _

- by Dr. Ebenezer Emmons, with the area of Berkshire, Rensselaer, aide

ae 1): 0 a eerie ga A THE CAMBRIAN. EST. State

Pd

PROBLEMS OF NOMENCLATURE AND CLASSIFICATION, Res:

The name.—It is still a ‘debatable question with a few geologists,
whether we shall follow the present general usage and use the name —
Cambrian group, with the area of Cambrian in Wales as its type and >
the descriptions of Prof. Adam Sedgwick as the classical description of | 4
the group, or, in opposition to this, adopt the name Taconic, proposed

Washington Counties, east of the Hudson River, in New York, as the —
type, and the papers of 1842 and 1844 of Dr. Emmons as the classical -
description of the group.
While recognizing the fact that the name Taconic has certain ctaicnil a
upon the sentiment of Americans, I have stated elsewhere that I think —
the interests of geology are best served by adopting the term Cambrian, — a
as has been done by the great majority of geologists. a
The limit of the group.—The delimitation of the upper limit of the —
group by geologists who recognize it as distinct from the superjacent —
Silurian (Ordovician) has varied to the extent of placing the arenaceous _
- deposits of the shore line, or the strata referred to the Potsdam sand- —
_ stone, in the Silurian, or including the superjacent Calciferous forma- _
tion in the Cambrian. To a large extent this difference of opinion is
based upon the evidence of the local physical conditions of sedimenta- —
tion, and not upon the included faunas. If we adopt as the principle of 7
Classification that the delimitation of the great geological groups must. —
rest upon the broad zoological characters of their included faunas and |
not on local stratigraphic breaks between certain series of rocks, or on
local differences of sedimentation, the line of demarkation between the
Cambrian and Silurian (Ordovician) is to be drawn where the marked: —
characters of the Cambrian fauna give way to those of the Ordovician. @
‘That this principle is the only sound one upon which to base the delim:
itation of a group is proved by the fact that there is no other relatively .
- constant character upon which to rely in geologic classification. Thats
- it is often arbitrary is known to all working geologists. _ a s
The line of demarcation along the northern and eastern sides of the 4
Adirondacks is between the upper beds of the Potsdam sandstone and 4
the calcareous layers of the Calciferous formation. On the south side, —
‘in Saratoga County, it is drawn in a series of limestones, where the —
characteristic Upper Cambrian fauna disappears and the types of the —
Silurian (Ordovician) fauna appear. In western Vermont, 20 miles
from where the division is made between the Potsdam and Calciferous —
formations, the line is drawn in a series of black argillaceous shales, ©
somewhere between a horizon carrying characteristic Upper Cam-
brian fossils and another horizon some distance above, in which —
- characteristic Calciferous fossils are found. In the Southern Appala- —
chian Province,in East Tennessee, the line of demarcation is not at the
base of the limestone series, but at a point in the lower portion of it, —

Ay .
fe
+

, .
3 ~ |
— _ * . ee ny “
Se : “< t ag
b a oe oo hk i aa a “

he — ee

PROBLEMS FOR INVESTIGATION. - — 8389

“where: the characteristic Upper Cambrian fauna disappears and the
Sil urian (Ordovician) fauna begins to predominate. This same prin-
ciple of demarcation is followed in the limestone series of central
& Nevada, while over the interior continental area it is largely drawn at
the summit of the sandstone carrying the Upper Cambrian fauna and
. at the base of the limestone in which the Calciferous fauna occurs. In
& ‘some instances, however, the Upper Cambrian fauna extends up into
4 _ the Calciferous beds, and in such the line of demarcation occurs in the
Be wettctore zone.

_ It is not always possible to delineate on the map such close lines of
Re harsation within a formation, and for the sake of convenience it
may be well to map the formation by their lithologic characteristics and
_ describe in the text the line of delimitation between the groups. When,
however, the line between two groups occurs in a limestone, as in the
we teeny limestone of the Hureka district, Nevada, and there is sufti-
. cient paleontologic evidence to demonstrate it, the line should be drawn

on the map at the point indicated by the faunas.

The problems in connection with the delimitation of the summit of

tne Cam brian group remain to be studied in nearly all porticns of the
% __ various provinces. In some they are fairly well settled, but there still

. _ remains much to be done in the way of collecting the Sania and study-

ing their verfical distribution in the strata.
| BS _Is the basal line of the Cambrian group at the lowest limit at which
the Olenellus fauna is found? Where this lowest limit occurs at the
a base of a conformable series resting unconformably upon pre-Cambrian
rocks there is no difficulty in answering the question. “But where it
: % occurs in the midst of a conformable series and there remain thousands
S of feet of sediments beneath the Ulenellus zone, as in Nevada and Utah,
_ it still remains a problem for consideration. On the general proposi-
e tion that I would not refer to the Cambrian any rocks beneath the
x -Olenellus zone, the subjacent strata of the western Rocky Mountain
> area were referred to the Algonkian in the paper reviewing the Lower
~ Cambrian or Olenellus fauna published in the tenth annual report of
4 the U.S. Geological Survey. I think, however, it is a question for dis-
E cussion and research, as the Olenellus fauna has a great vertical and
ee time range in the Northern Appalachian Province, while in the South-
ern Rocky Mountain Province it is limited to the very narrow band of

s strata at the summit of the siliceous series of slates and quartzites.

aq

-- That the question of how the Cambrian shall be divided in America
> still requires investigation, with special relation to the classification
x to be applied in the various provinces, is well known. The three pri-

_ mary divisions of the Cambrian (Lower, Middle, and Upper) are readily
recognized. in Newfoundland, and that one or the other of these divi-
p sions can be distinctly ere: in the other provinces has been
_ proved.
ee) in ake Interior Continental sthes only the Upper Cucabrian with

- i = * —n- & eo y <> SS vin ew Se» Q
: : ee, ee top Sed Me ag: as ne
. aes > ne Tat Les py ss eee
os tS ware i ? = 7 s » G r¢ ‘ ud >
ee” SIV : “THE CAMBRIAN. SR ed a
. ; ~ t * n e-- + & Je i
es , ee at “ae

its distinet sedimentation and fauna, i is ‘S<n0wn spits no other appears to ‘i
~ have been deposited. In the Appalachian Province, in Vermont, the
_ Lower Cambrian is readily separated by organic remains and astinedtt
tation ; but with our present knowledge it is impossible clearly to dis-
Boouieh between the Middle and Upper Cambrian. The same is true |
throughout the Appalachian region, except in the Adirondack sub-_
province, where the Upper Cambrian is well developed. In the fer
Mountain Province the Lower Cambrian is distinctly developed, but the
Middle and Upper merge more or less into each other. The ‘problemi
-in this connection requiring investigation are clearer delimitations of
the Middle and Upper Cambrian in the Appalachian and Rocky Moun- 3
tain Provinces, both by the careful study and comparison of the sec.
tions and the collecting and differentiation of the faunas. > 7
It is not anticipated that uniformity will be found to exist in each 0 2
: the primary subdivisions ; the sedimentation of the various provinces
ig too unlike. The three divisions will have to be used, if at. all, in a
somewhat arbitrary manner in some of the areas, just as the greater a
division of the Cambrian is arbitrarily separated from the Silurian
(Ordovician) where no physical line of division is apparent. We recog-
nize the Cambrian group as a convenient means of classification, but
its subdivisions must be controlled by the needs of the local geolog: ist
and not used unless distinctly recognized. ~ |

a OHAPTER VL

=4 : CRITERIA AND PRINCIPLES USED BY AUTHORS IN THE corR-
age LATION OF THE VARIOUS PARTS COMPOSING THE GROUP,
Saige OBSERVATIONS ON SOME METHODS OF CORRELATION.

a
&

w 4
“V4

Ro HISTORICAL NOTES.

2 earlier Rccdicee geologists Gux their first views of classification
Sat giteiplee of correlation mainly from European authors. Among
th he latter Dr. John Woodward said early in the eighteenth century in
s “ Natural History of the Earth”:
at the stone and other terrestrial matter in France, Flanders, Holland, Spain,
,G my, Russia, and Sweden were distinguished in strata or layers as it is in
and die shioes strata were divided by parallel layers; that there were inclosed
the stone and al) the other denser kinds of terrestrial matter great numbers of the
Is and other productions of the sea in the same manner as in that of this island.’
s is one, of the earliest correlations of stratified and fossiliferous
- It is ernde and indefinite as compared with modern correlation,
tthe general method of comparing stratified fossiliferous rocks be-
2 they : are stratified and fossiliferous was inaugurated.
Dr. Abraham Werner, in Germany, gave systematic form to deserip-
e geology in the latter part of the eighteenth century; while about
2 same time Prof. William Smith, in England, applied organic re-
ains in geologic investigation, and correlated formations in various
— of the British islands by their contained fossils. A little later
_ Baron George Cuvier was establishing in France the great principles
the succession of varying organic remaius in the strata and their
dation from living forms.

AMEBERICA.

_ Macture In Ammetion Mr; William Macture was among the first to
ie advantage of the principles of classification enunciated by Dr.
= , and we find the correlations made by him in preparing his
__ geological maps were based entirely upon lithologic and stratigraphie

Wi
a | 4
® 7 7
Wate Pi:

‘

iY +, m 4

¢

-

_ vidence. This is stated in the first paragraph of the introduction to
his paper:*

a system. So far as respects the classifiea-
"tion and arrangement of names the Wernerian appears to be the most suitable, first,
it is the most perfect and extensive in its general outlines, and secondly,

_ - ;

as | Esesy towards 2 Natural Histo. 7 of the Earth and Terrestrial Bodies. London, 3d ef, 1723.
a ue the Celery of the: Unsted States explanatory of a geolesical map. Am. Phil See.

ool

‘the most correct elucidation of the general exactitude of that theery as rehire the $

ognized by a separate color, : a

the Transition into five varieties, the Secondary into twelve, and the —

- face, describing exactly the different rocks with their immense variety. /%

_ 4 An index to the Geology of the Northern States, with a tadelities section from Catskill | Mountain

he at et ee nang ba a ee 6752 ee Shs alt ae Roi Le tac at oe ot ict a
7* -_ a ~ ; ole re. « eh ves oe 4 c ae
‘ “ - - oo > “ » a < —

a. a»: he | >> ys = re “ ‘> 4 ‘a ‘3 —- te — OTe = -

Soe Mie) en oe THE CAMBRIAN. = SS er

the nature and relative situation of. the minerals in the United 1 States, while megs are
certainly the most extensive of ‘any field yet examined, may perhaps be found to be 2

a

relative position of the different series of rocks.

On the map four great classes of rocks are recognized: cians I, Primi. “
tive rocks; II, Transition rocks; III, Secondary rocks; IV, Alluvial —

rocks. The presence of rock salt in the southern Appalachian i is rec-

In the text! the Primitive rocks are divided into fourteen varieties,

Alluvial into seven. In traversing the country Mr. Maclure noticed the
presence of any one of these rocks at their various outcrops, and —
thus correlated the geological formations that presented similar
characters. In the second edition of his work? two methods of e ex:
amining and correlating the rocks are given: os:

The first, the accurate investigation of a small portion of the sur- a

of arrangement and position of their component parts, detailing the |
changes, accidental or natural, constantly occurring in their relative _
situation, and endeavoring to reduce the whole to some regular series —
of arrangement. This method necessitates the reunion of a great noni j
ber of those portions before any correct general idea can be formed. o
The second, beginning with the great outline, traces the limits which |
divide the principal classes of rocks and their relative situation and
extent. Mr. Maclure favors the second, stating:
In tracing the outlines of the different formations in most countries there ts eas |
confusion and embarrassing description necessary ; the limits once ascertained, a few
pages define the boundaries and explain the relative situations to the comprehension — A
of every reader. .
Eaton.—After Mr. Maclure, Prof. Amos Eaton was “the most impor:
tant factor in the shaping of the methods of geologic work i in America. |
By his various publications and his influence as a teacher he outlined
the methods and formulated the general principles upon which geologic —
investigation was carried forward for nearly two decades. The correla-—
tions made in his earlier works were based entirely upon the lithologic —
characters of the rocks. Believing in the Mosaic cosmogony, he 6x- "9
plained the phenomena he observed in the structural relations of the —
rocks by the giving way of the foundation of the Old World prior to 4
the flood. He says :*

While this tremendous crash of nature was going on, scales of various thickesiaall +
from the various strata were shot up, detached, and broken, which gave formation to
our surrounding hills, the ragged cliffs of the Catskill, and the bleak brow of the _

AS
5

os

1 Op cit:, p. 412. ; ee.

2Observations on the Geology of the United States; with remarks on the Enel: effects that : may_
be produced by the decomposition of the different classes of rocks on the nature and Orne of soils. te :
Am. Phil. Soc. Trans., vol. 1, new ser., 1817, pp. 1-91.

3 Op. cit., p. 9. p 2

to the Atlantic. Leicester, 1818, pp. 48, 49,

-

en from various causes since the great deep retired.

r, During the deluged state of the earth many species of animals were robabiy de-

“stroyed, For we continually find the petrified remains of epepier of animals now

- to ails extinct. —

From the latter eceaicahich it is quite evident that at that time he
Sax not consider fossils to be of any value in the correlation of the
rocks. | In the next edition of the Index ! his theories of the origin and

> first condition of the surface and position of the rocks are omitted, and

; classification of which was lithologic and based on the views of Dr.

_, Werner. His more extensive work of 1824? shows that the correla-
~ tions made between the rocks of the Hudson and those west of the
3 Hudson, along the line of the Erie Canal, were based mainly upon their
“4 __ lithologic characters. For instance, the Calciferous sandrock of the

Bf ‘Mohawk Valley, in the vicinity of Little Falls, New York, was traced
E westward in the vicinity of Utica and eastward down the Mohawk
ee: _ Valley to the vicinity. of Schenectady, and then correlated with a Cal-

2 * was, made upon the lithologic character and the stratigraphic succes-
i ~ sion ‘of the rock masses. Its defective character is shown by the fact —
: that the Calciferous sandrock east of the Hudson is of Lower Cam-

\ CORRELATION | 393

_ amore thorough description is given of the various rock masses, the —

x ° -_ciferous sandrock. on the east side of the Hudson. This correlation

brian age and that west of the Hudson is of Silurian (Ordovician) age. ©

SEN
=

Bes: - Classification and correlation on the basis of lithologic character and
- stratigraphic succession was continued by Prof. Eaton in his work of
a7 18287 and again in his text-book of 1830.4 On the map accompany-
ing the latter all the quartzose formations are colored yellow, all the
a ~ calcareous formations blue, the variegated sandstones red, and the sub-
Bi >. ordinate rocks green. By this the primitive inustanea of the Adi-
— _rondacks (Algonkian), the Lower Cambrian limestones of Washington
iS ~ County, the Calciferous-Chazy-Trenton limestones of the central por-
tions of the State, and the Lower Devonian limestones of the Upper
| Helderberg are all placed under one color.

_ In 1832° he introduced a new heading into his Text Book, as follows:
oa Organized remains as auxiliaries in the determination of rock strata.”
— this he a eae ’

See vse:

al

tags met

Fae

Siete

vf pe EA

be An Index to the Geology of the Northern States, 2d ed., 1820, pp. 286.
ate 2A geological and agricultural survey of the district adjoining the Erie Canal, 1824, pp. 163.

ms 3Geological nomenclature, exhibited in a synopsis of North American rocks and detritus. Am. Jour.
es: oe ‘Sei., vol. 14, 1828, oppo. p. 144, pp. 145-149, 359-368.

© #Geological text-book, prepared for popular lectures on North American geology; witb applications :

Bt pee cultare and the arts. Albany, 18380, pp. 64.
aa. * "8 Geological text-book for aiding the study of North American Geology ; being a systematic ar-

Van Rensselaer. 2ded. Albany, 1832.
*Op. cei P p. 25. - “ -

pes pt

iB _ rangement of facts, collected by the author and his pupils, under the patronage of the Hon. Stephen ;

\

~

‘

—_

‘ Py | =e es AP 6 ore Le ‘tore a eS ae, ae »s

dep a er Sok care Olan hong MO pn my rea
Tew ce La ae heii, —i =

: a at het, Sa mies S SF Ge Sean

=< & Racal = ay be ‘ - wo, ae
2 ; pe

ore eas vs ‘ Pe P THE CAMBRIAN. y Le ee

in the rocks the foligwine passage occurs:

The geological deposits of this country (and probably those of the eastern. conti- .
nent) exhibit grounds for conjecture if not absolute demonstration that the surface -
of the earth has undergone five general modifications, which no animals survived. | ‘
Four of these modifications were followed by as many new creations of animals. Also — :
that two new creations of animals succeeded tbe final depositions of all regular strata, — =
In the whole, there appears to have been five creations of animals at least (perhaps — |
ten) since the primitive m ass of the earth was formed, and a long interval sueceeded |
each creation. . By

It is also said that the “ remains or impressions of plants are limited — es
to coal and coal formations whose relative position is indicated by their ‘3
_rocky associates; the determination of rocks by their animal relics
serves as an index to the position of coal measures or beds. In this”
concise selection of the most essential relics animals alone will b a 33
noted which have no backbone nor brains” [invertebrates]? == z.

Under the title of ** Geological Equivalents” Prof. Eaton mentions —
that relative position and mineral constituents were deemed sufficient 3
by Werner for determining geological equivalents. As relative position —
is the basis of the science, all other circumstances have always been
received as auxiliaries only so far as classification is concerned.’ He — ;
reasoned that as rocks can be traced more or less continuously through- —
out New York and Pennsylvania the data used by ioe are of
value; but— | .

From a consideration of the cases here referred to, intrinsie harasal more definite a
than any left us by Werner seem to be essential to the progress of the science. The —
enumeration of mineral constituents of rocks can never be satisfactorily spoils 4
Unorganized matter presents but few characteristics. Naturalists find it a more dif- —
ficult task to describe by external characters about two hundred and seventy species
of minerals than fifty thousand species of plants and a Ban larger number of ani

mals. . sep
It is a subject of high congratulation to students in geology of our day-that the
illustrious Cuvier, aided by the Brongniarts and their coadjutors, have extended the —
science of organic nature to the science of geology. We are no longer limited to the —
enumeration of mineral constituents. We find the same organized remains associated if
with equivalent strata in every part of the earth, though they often extend in to

several adjoining strata, which are probably contemporaneous or nearly so.4 S ;
He then proceeds to classify the strata as known to geologists of both
continents by means of some of their organic associations in North |
America® ‘ = :
A few months later he published a paper on ‘ Four cardinal points,
in stratigraphical geology established by organic remains,” say ing:

If the identity of the Granular, the Metalliferous, and the Oolitic calcareous rocks “a
and of the Teriiary marls are established on both continents all intervening ‘strata —
may be ascertained with great facility. I think that a reference to the following —
facts will be sufficient to establish their equivalent characters at least.° Meh

1 Op. cit., p.48. - 6Op. cits, pp. 136-138. > . -
2Op cit., p. 25. Four cardinal points in stratigraphical geolog
3 Geological ailivalenta: ea Jour. Sci., vol. 21, established by organic remains. Am. ¢ ‘ eo :%

1832, pp. 132-138. _ Sci., vol. 21, rh 199. Spit Fake
4Op. cit., p. 134 : i ee

- > —

The ‘frst eardinal péikt is the Granular limerock “the only lime-

ele
a

- Under this headin g he correlates the limestone at Trenton Falls and
_ most of the limestones of New York. The third cardinal point em-
braces the Oolitic series or Calcareous rocks, and the fourth the Ter-
_ tiary marls. These correlations of Eaton were erude, but when re-
_ fined by the geologists of the New York State survey the first three
A “gered. the basis for the correlation of the lower and middle Paleozoic
rocks of the continent.

Bigsby.—The earlier work of Dr. J. J. Bigsby was apparently un-

ae known to Eaton. The former used organic remains in a very general

“ee

hs .??
“ > wae ra, fhe
Pi

7s
‘

par
La >.

oat ¥

~ pended upon the lithologic characters and stratigraphic succession.
es In an article entitled “A list of minerals and organic remains oe-

*

A aby

the limestones and sandstones of the eastern and western parts of
“Canada, Of the limestones he says:

c ;

= ne Their relation to the subjacent rocks and uniform similarity in structure and con-
@ re tents, mineral as well as organic, seem to indicate that the beds of limestone, extend-
ing with few or no interruptions from Cape Tourment, below Quebec, to near the
Falls of St. Mary, are the effects of a contemporaneous deposition; and further,
= that they are the representatives of the Mountain or fae aeons limestone of Eng-
3 : land.

~~ .I make these statements with extreme diffidence, being in some degree aware of
a _ the difficulties of the discussion, of the existence of contradictory facts, few but
__— weighty, and of the defective state of our information respecting the vast calcareous

formations of North America.!
_ The reference to the secondary limestone of the St. Lawrence and
the lake region is as follows : R

The limestone now described abuts on one of the older rocks directly, or with the

- interposition of another borizontal stratum, and by far the most commonly on
gneiss, which I have strong grounds for believing to be of the same age and general
characters throughout the whole of the districts under consideration. It is in-
- eumbent directly on gneiss in the bed of the river St. Anne, near its upper falls,
a . in the seigniory of St. Feriole, Lower Canada; at Montmorenci, not far from ‘the
Bp - natural steps,” but only seen in time of low water; at and near Point Henry, close

*/ > a!
i t
t re

= «>a

Fo Se
=<} +
ll

- ahs sf
tgs

eee to Kingston, Upper Canada; and in many places on the north coast of Lake Huron. ~
- In the last-named locality it rests directly, in several instances, on a beautiful snow-_

oe white transition quartz, which occupies the main shore in steep hills, 400 and 500
feet high, from near the French River to the River Le Serpent (70-80 miles). The
% immediately subjacent rock at La Cloche and on the isles north of the Manitoulines,

Gt, Vig Te ET AS ree See re Pages a RG eos NET ERE On ce ark ee

Lap tg OO a can : < oe eee

: St odie , . rh 8 SP A : wie
ee CORRELATION. | BSS.

- rock which is always destitute of organic remains.” The second car-
a dinal point is the Metalliferous, Mountain or Carboniferous limerock.-

et cae in the Canadas ” he remarks upon the extent and relations of —

ke in the same lake, is sometimes a highly inclined greenstone. Near Montreal it _

-manuer to correlate the strata of England and America, but also de- .

vowel _ overlies directly crystalline trap, containing augite, zeolite, mica, feldspar, ete.

bs , But ordinarily a sandstone, gray wacke, or a.conglomerate of quartzose or calcareous

_ a ‘materials is interposed ; also in horizontal layers. It is to be remarked (en passant)
< that much the greater part of the graywacke of Lower Canada does not belong to _

oe
,

- this deposition, but is conformable to the mica-slate, gneiss, efc., ranging along the
north shore of the St. Lawrence, between Quebec and the river Saeuenhy.

“

» Fae e

Aa ae re list of mineral and organic remains occurring in the Canadas. Am. Jour. Sci., vol. 8, 1824, pp.
ee cyet 3
Bi MP -

* * *

-—

: a in -
=. . * f ate 4 we + TA
: Vs 7 u bs

896° 8 2 ee CAMBREEN.

The sandstone, which is beneath the limestone from near Kingston, Upper Canada,
to St. Anne’s, 26 miles northwest of Montreal (174 miles), is white, but with fer. P
_ruginous spots and clouds, hard, fine grained, without cement, and contains: thi ck
layers of large and small nodules of crystalline quartz, diapanta in horizonal lines.
It forms cliffs an hundred feet high in the Lake of the Thousand Islands, which rest
on the very small-grained gneiss (often a granite) which abounds so in the north and
northeast and passes largely and frequently into primitive white quartz rock, thus»
_ disclosing a possible source of the sandstone and quartz nodules. Where clay is he.
‘cement an argillaceous sandstone or graywacke is furnished. The former of these | Py
have never seen in contact with the inclined rocks. It occurs very distinctly in the e
chasm of the Niagara, the lower strata of which (and particularly those on whic
Queenston stands) are almost ferruginous clay. The nearest primitive is on the north
shore of Lake Simcoe, 90 miles off. From the nature of the organic remains and other ee
contents of the limestones covering this sandstone, I am inclined to believe the latter
to be the old red, which is often thus intermixed with argillaceous matters. At Dun-
kirk, on the ath side of Lake Erie, Mr. Hulbert has bored through these rocks to the |
depth of 682 feet (117 feet below the surface of the Atlantic) and without meeting with ©
salt. The above observations apply to the fine sections in the bed of the Genesee —
River; but I have not sufficiently examined the fossils in the limestone of that locality.
Its AES has large but indistinct casts of what I suppose to be encrinites, but
which may be vegetable, but in either case resembling the Old Red sandstone. It ~
may be added that it is on the same level with and not very far from the sandstone
of the vicinity of Kingston; but similarity in level taken by itself is not an unerring ©
test of similarity in age. In one part of a district or lake granite, gneiss, etc., may —
attain a given elevation and be there covered with graywacke only; while in an-
other and not very distant place these rocks may not rise to within some thousand —
feet of that height, and be buried under all the succeeding strata up to the Crag )
above the London clay.! a
A conglomerate wholly caleareous occurs in situ near the foot of the Long Sault
of the river Ottawa, and at the Coteau du lac, 3 miles below Lake St. Francis, com- —
posed of angular and rolled masses, sometimes very large, of fine granular limestone — :
light brown and blue, imbedded in a dark brown paste. A similar rock occurs with ~
_the limestone about Poughkeepsie, in the State of New York, and at Aubigny, oppo- :
site Quebec, interleaved with clay slate and gray wacke, highly inclined, and having
a southwest direction. " a

¥-

The elements of correlation suggested in the preceding quotations |
include lithologic resemblance, similarity of level in a given area, strat-—
igraphic succession, and the presence of organic remains. a

At a later date ne Bigsby noticed in the conglomerates on the south me:
side of the St. Lawrence, opposite Quebec, the presence of tnilobibeng ‘
encrinites, corrallites, and other fossils, and, on this account, considers —
the formation the equivalent of the poorer ho limestone of the —
English geologists. ° Ke.

James.—One of the earliest extended correlations in neue is tha e:
of Dr. Edwin James.‘ In his remarks on the sandstone of the western =
part of the valley of the Mississippi he first describes in detail the red
sandstone.° He states that this rock is the lowest of the Loreen a

2Op. cit., p. 81.
On the geology of Quebec and vicinity. Proc. Geol. Soc. London, vol. 1, 1827, Dp. 38.

5

10p. cit., pp. 78-80. eT hi a
, %

ft

4Remarks on the sandstone and Floetz trap formations of the western part of the valley oe tial sg

_ Mississippi. Am. Phil Soc. Trans., vol. 2, new ser., 1821, pp. 191-215. Peet a.
5 Op. cit., p. 204. Sa 3
e ~ = 4 - J -' ~ Lg %

ON rex Sark: Eeaiabos from many parts of the strata on the Canadian
Ri ver are entirely similar to those quarried in New Jersey and used

7

m in great quantities in the cities of New York, Albany, etc., for build-
ing.

a Whether this sandstone is in all respects similar to the ‘Old Red

3 sandstone’ of Werner, which makes so conspicuous a figure in the

systems of certain geologists, we are not able to say. It, however,

be certainly occupies a place similar to the one which has been assigned

to that rock.” In a foot-note referring to this statement it is said

This red sandstone is first found on the waters of the lakes on the strait between
Lake Huron and Lake Superior, and forms the fall called the Sault de Ste. Maria.?
_It also occurs in the Catskill Mountains and in the Salt District in the western part
s “of the State of New York, having a similar relation to the secondary rocks in that
quarter. * * * The red sandrock now under consideration appears at one place
~ with every character requisite to place it among the rocks of transition, at another’
4 it is manifestly secondary ; yet its continuity may be traced through minute shades

' of gradation or by a sudden transition from one of these points to the other.?

d
F
,

Fe _A review of the preceding remarks indicates that Dr. James sup-
posed the Jura-Trias sandstone of the eastern foothills of the Rocky
_ Mountains, the red sandstone of the Lake Superior region (Algonkian),
- the eastern New York sandstone (Upper Cambrian), and the New Jersey

/ Trinasic sandstone were of the same relative geologic age asshown by

_ their lithologic characters and supposed stratigraphic position.

Bakewell.—The publication of the American edition of Mr. Robert
F Patenclls Geology in 1829 was an important contribution to American
~ geologic literature. It presents an account of the geological distribu-

. _ tion of organic remains as then understood and the general principles

_ of geology as known to English geologists.

is In regard ta correlation by fossils Mr. Bakewell Says:

ae “With respect to fossil conchology he is inclined to believe that the attempt to iden-
tify the strata of distant countries by the isolated occurrence of any particular species
of shell has been carried further than a sound induction from facts or analogy would
* warrant. His opinion on this subject, given in the second edition of this work, he
a here insert: ‘‘It may be doubted whether the occurrence of similar organic
_ Temains is sufficient to identify strata inglistant parts of the globe; for could we
: admit that strata are universal formations and extended from the frozen to the tor-
rid: zone, it seems more than probable that the animals that lived on any one partic-

; flues stratum would be of very different species in different latitudes.” * * *

- Instrata belonging to one formation and in adjacent districts, the existence of cer-
te atin, shells, whether we regard them as distinct species or as varieties, may be of use
in identifying any particular bed; and in distant countries where we find the same
remarkable species of shell kuiboiatad with any other remarkable species in consid-
sy erable numbers it may serve to identify a particular rock formation, where the min-
eral character of the rock may be very different from that in which the observer has

eof. ee 1Op. cit., p. 205. ig : ? Op. cit., p. 206.

bie Peal

398 = THE CAMBRIAN.
been sanhatnan to bet with ihem. The occurrence of a cansidonatiiag acid of E
gryphex, the Gryphea arcuata in a bed of blue clay in the mountains around the

Lake of Annecy in Savoy, served the author as a key to discover to what formation <
_ the caleareous strata peore ets) when their mineral characters would have indicated —
@ more ancient series.! ‘

A
a

De la Beche.—In 1832 an édition of the Geological Mannal? of De 1s
Beche was published in Philadelphia. In the section upon the classifi- 3
cation of rocks we find the following remarks | npoy classifiation by 4

organic remains: ; eS a

To propose in the present state of geological science any clnasiiextian. of rocks a
which should pretend to more than temporary utility would be to assume a more
intimate acquaintance with the earth’s crust than we possess. Our knowledge of — a
- this structure is far from extensive, and principally confined to certain portions of — 3
Europe. Still, however, a mass of information has gradually been collected, partic- a
ularly as respects this quarter of the world, tending to certain general and important

conclusions, among which the principal are, that rocks may be divided into two |
' great classes, the stratified and the unstratified; that of the former some contain | .
organic remains and others do not; and that- the nonfossiliferous stratified rocks, ‘
as a mass, occupy an inferior place to the fossiliferous? strata, also taken as a mass. 3
‘The next important conclusion is, that among the stratified fossiliferous rocks there —
is a certain order of superposition, apparently marked by peculiar general accu- —
mulations of organic remains, though the wineralogical character varies materially, -
It has even been supposed that in the divisions termed formations there are found ~
certain species of shells, etc., characteristic of each. Of this supposition extended —
observation can alone prove the truth; but it must not be supposed, as some now .
do, that in any accumulation of ten or hare beds, characterized by the presence — 9
_ of distinct fossils in a given district, the organic remains will be found equally char- ;
acteristic of the same part of the series at remote distances. ; 3

To suppose that all the formations into which it has been thought advisable to %
divide European rocks can be detected by the same organic remains in various dis-— ll
tant points of the globe is to assume that the vegetables and animals distributed —
over the surface of the world were always the same at the same time, and that they —
were all destroyed at the same moment, to be replaced by a new creation, differing
specifically, if not generically, from that which immediately precededit. From this —
theory it would also be inferred that the whole surface of the world possessed an uni- —
form temperature at the same givenepoch. | ‘ Jom

It has been considered, but has not yet been sufficiently proved; that the lowe a
rocks in which organic’ remains are found entombed show a general uniformity in 4
their organic contents at points on the surface cousiderably distant from each other,
and that this general uniformity gradually disappeared, until animal-and vegetable.
life became as different in different latitudes, and even under various meridians, as
it now is. How far this opinion may or may not be correct can only be seen when |
geological facts shall have been sufficiently multiplied ; but it is one which demands ~
considerable attention, as the classification of fossiliferous rocks greatly depends upon. r
it. Should it eventuality be found to a certain degree correct it would not be at va- —
riance with the theory of a central heat, which having diminished permitted solar
heat and light gradually to acquire an influence on the earth’s surface.4 a

-

y

Numerous, other European works soon came into the hands of the ig
American geologists, among them the earlier editions of Bakewel

1Introduction to Geology, Robt. Bakewell, Ist American edition, New Haven, 1829, pp. a, 33.
2Geological Manual, Philadelphia, 1832.

® The term fossiliferous is here confined to organic remains.
‘Op. cit., pp. 33, 34.

Lye Si Mantell, ond varions French and German ay Ste Their influence
Stains by the rapid development of stratigraphic geology based upou
the pr principles: established in Europe. Of the means of correlation avail-
able to Prof. Amos Eaton in his earlier work he says, in 1839:

3 ‘Eaton. —When I commenced my geological surveys the application of organized
_ remains for demonstrating strata was not studied in America. I had become ac-
x ~ quainted with no method for determining the. character of such strata but that of
tracing them separately through a vast extent of country and then comparing their
2 _ general characters. For this purpose I traveled some thousand miles at my own ex-
: _ pense and with the liberal aid of students of Williams College, with Prof. Dew ey at
e e dhete head, where I was employed more than a score of years since by the authorities
__ of the college to introduce the natural sciences. Afterwards I traveled more than
wi “27, 000 miles on geologizing tours at the expense of the Hon. Stephen Van Rensslaer,
> and I was always aided by several assistants and competent students. Had the ap-
_-Plication of paleontology been then as well understood as it now is I could have
settled the characters of most rocks as well in my closet by the aid of specimens,
- - Bat it is a true remark in your last journal that strata must have been first settled
according to the method to which I was compelled by ignorance to submit, before
os - the service of organized remains could be successfully employed. In this country no
* - material: progress had then been made in the study of organized relics, and even now
we have very few good paleontologists.!

= porte > NEW YORK SURVEY.

s2oekhe geologists of the New York State survey systematized the work

_ of the geologists who preceded them and established a standard section

of the lower and middle Paleozoic formations of New York. On this
account it is desirable to examine the principles of correlation men-
- tioned by Messrs. Conrad, Hall, and Emmons and to notice the extension
of. the nomenclature of the veuations of the New York section to vari-

ous portions of the continent.

ek -Conrad.—As paleontologist of the survey Mr. T. A. Conrad made the

: - following comments upon the use of fossils in the correlation of strata :?

—

ae There isa strange misunderstanding of the method of applying organic remains
in the division of series of strata into formations and the identification of widely
% _ separated rocks by the zoological characters of each. In the January number of the
_ New York Review the opinion is advanced that the ‘‘Calymene blumenbachii ought
to be carefully sought for in the rocks which are said to correspond to the Dudley
- period. Unless it is found, or some other consideration is introduced, can it be be-
~ lieved that fossils are a Fetintgetar’ evidence of the age and place of rocks?” The
¥ line of demarcation between rocks of different age has never yet been drawn with
- any accuracy by the aid of paleontology, except by the consideration of groups of
_ species, one or even a few species having no weight whatever in the determination.
Thus the shell termed Terebratula Schlotheimii dates its existence with the Trenton
“Jimestone, and reappears in three of the latter formations of the Silurian system. Or-
_ this testudinaria, Dalm., is peculiarly characteristic of the Trenton limestone, by its
: Beaeaost invariable presence and extreme abundance, and yet it is also found in the
= _ limestone of the Helderberg, a formation of a far more recent origin. But, although

‘ a fow species may have been continued through a succession of geological eras, the

“ — ee

a -_ 1Cherty limerock or Corniferous limerock, proposed as the line of reference for State geologists
_ of New York and Pennsylvania: Am. Jour. Sci., vol. 36, 1839, p. 67.

tg *Second annual report of the paleontological department of the survey. Third annual report of the
» geological survey of New York, 1839, p. 58. pena

: a eee

ot ae .

CORRELATION. Be teed 995-.

°

/

- identity of formations can never again be called in question by a geologist who de-

- mere seams and layers. It is also stated that the catalogues of organic

/

_ with the Rochester shale, and the Wenlock limestone with a limestone

- is also established, that whilst some genera and many species are restricted to a sind He 4

black slate of the Mohawk, characterized by a Sot Ss trilobite, ‘Triarthrus, whieh

pity TS Bh oa a ER Be ha ha SO Ss or eC eee te
NESS SORT Wats SEAS eee ae
, “ek yey - + * ¥ : : rs RY! “ae o> 4. oN
i> 4 7 Vl gS ea wr : ~~ 1 opt oe i he em " fit a ‘. + ‘& ; yes
a ae Kaila ‘THE CAMBRIAN. Secs

groups are widely distinct, and their value in ‘aahacna ide ide ‘domnarative: age al 2

serves the name. FG Sal ae

Attention is called to the fact that no observer has yet ‘cath the
line of distinction between the Trenton and the newer limestone super: |
imposed upon it in Ohio and Kentucky, because the similarity in min-~
eral character and color is so perfect, and both formations thin out into —

remains of the Silurian system hitherto published in Europe are cal- —
culated only to mislead and confound the geological inquirer, as they
are far too vague.’ a
In 1840 Mr. Conrad instituted a series of comparisons of formations —
of the New York section with those of England, based upon the fossils.
contained in their respectative formations. He compares the Caradoc —
sandstone with the limestone of Trenton F'alls, and the Wenlock shale

developed in the Helderberg Mountains.?
In the fifth annual report on the paleontology of Ney York we ‘find
the following remarks applied to correlation of the rocks of the State 3 4

The horizontally and undisturbed condition of the strata have enabled us to trace
their sequence or order of superposition with comparative ease and greater accuracy
than can always be obtaiued in regions where the formations have been much —
inclined or distorted, These divisions or series are usually composed of various —
layers, as compact limestone associated with friable shale, sandstone alternating with ¢
argillaceous shale, etc., and these modifications of their mineral constituents are—
generally accompanied by some variation of the organic contents; new species have *f
been introduced, or more ancient ones have disappeared. But it is only at the june- “i
tion of two formations that each group of organic remains is not perfectly distinct
and characteristic, a mixture of species sometimes occurring which proves a gradual —
transition from one era to another, and gives rise to some uncertainty where the —
exact line of demarcation should be drawn. This fact opposes the idea someting ;
indulged by speculative geologists, that sudden convulsions of the earth’s surface vs
have been the cause of exterminating forms of life, and the introduction of others. to. Pre
supply their place. The change seems rather due to alteration of temperature in the bs
water, whatever new physical conditions of the earth resulted at the same time. ay
Such phenomena, however, do not interfere with the general distinctive characters” a
of the stratigraphical divisions adopted in this work. It is now, I believe, an undis- “-
puted point in geology that certain groups of organic remains belong exclusively to | :
certain formations, and that these strata, in a general way, may be known and com- | .
pared by the same groups of genera, if not species, in every region of the earth. ie”

gle formation, others have originated at an early period and continued to exist s
throughout a large portion of the time occupied in the deposition of asystem or series |
of formations. * * * a

The color and even mineral character of a formation usually varies areatly over an a
extended region, but it may be recognized by its fossil contents; for example, the

“

1 Op. cit., p. 59. 55°

2Qn the Silurian System, with a table of the strata and characteristic fossils. Am.J our. Sci., vol. ae >

1840 pp. 87-91.
3 Fifth annual report on the paleontology of New York. Fifth Annual Bepers; of the Geological

Survey of New York, 1841, pp. 25-27. Albany.

E ae Bee 2 yay -

lever been knowin to occur in any other sbologiont position, is ronraeeniadl by a
b-colored shale in the vicinity of Cincinnati, Ohio. There also the equivalent or
inuation of the black limestone of Draiicn Falls is of a gray or pale hue, and
be known.as the same rock only by its organic reliquis. The Caradoc sand-
tone series of Wales is represented in New York by limestone and slate in proportion
ae et to the arenaccous strata.

ow serve as standards of comparison for the purpose of correlation was
enunciated by Prof. James Hall very clearly in 1839, as follows:

A . Everyone who has studied rocks even partially is aware of the insufficiency of
ie 1 ineral or lithological characters for giving nomenclature, and the many errors into
* | which he may be led, whether in his own researches or by the mistakes of others. So
likewise in the present state of our knowledge we are unable in all cases to give

: and i in some may possibly be absent. It thus becomes a desideratum to distinguish
_-Tocks by names which can not be traduced, and which, when the attendant circum-
stances are fully understood, will never prove Paltuatswy, The basis of this nomen-
® -clatare is derived from localities, and the rock or group will receive its name from

the place where it is best developed.!
& aS
es He then proceeds to name the “Rochester shale” from Rochester,

New York, and the Lockport limestone from Lockport, New York.
; = In 1843, after stating the general results of an examination of a sec-
‘ tion.southwest from Cieveland to the Mississippi River, he wrote:?
From the facts here stated the conclusion seems unavoidable, that the character of
- fossils i is, or may be, as variable as lithological characters; in fact, that the species
spend in some degree upon the nature of the material among which they lived.
Fos characters therefore become of parallel importance to the lithological; and,
_ in order to arrive at just vonclusions, both must be studied in connection, and locali-
x ties of proximity examined. In the case of the Hudson River group of shales and
, iy andstones, in passing from New York to Ohio, the lithological character is almost
x entirely changed; and at thesame time also the most prominent and abundant fossils
. are unlike those of the group in New York. More careful examination, however, re-
veals the fossils which characterize this group at the East, and also at the same time
. _ some obscurely similar lithological characters. Similar lithological changes, accom-
ae panied by like changes in fossils, occur in more limited districts within the State of
New York.
The most marked and important changes, however, appear to be in the higher rocks
ve ott the New York system. The Hamilton group and Marcellus shale, which in New
York have a thickness of 1,000 feet, have diminished to 100 where last examined; and
ey from being the group most prolific in fossils, asit is in New York, it has seine en-
_. tirely barren of them. The rocks forming the Portage and Chemung groups, which
in their greatest development in New York are scarcely less than 3,000 feet in thick-
es ness, and in Pennsylvania much more, have in Indiana diminished to as many hun-
ag dred. The upper of these groups, from being extremely fossiliferous, has become
+s almost destitute of these characters, so that, at the farthest extreme examined, they
furnish but an equivocal guide. In these groups lithological character is more per-
a - sistent than fossils, and it requires ‘aknowledge of the superposition to identify them
as atisfactorily. The greater thickness of these sedimentary deposits, and the greater

* gt

a rat 1'Phird Annual Report of the 4th Geological district of New York. Third Annual Report of the
= _ Geological Survey of New York. Albany, 1839, pp. 288, 289.

we, 2 Notes explanatory of a section from Cleveland, Ohio, to the Mississippi River, in a southwest di-

; . rection ; with remarks upon the identity of the western formations with those of New York. Assoc.

. Am Geol: Trans., 1843, pp. 289-291.
oe hed 81——26

..
Bo

-
EN
7a

s9
re

“ a in ae ie a CORRELATION. oe ‘Ss 401

U. —The desirability of naming formations from typical exposures |

i "names from fossil characters ; for, though without doubt every group embraces its
peculiar fossils, yet in all localities these may not be so marked as to excite attention,

e |.
,

SE a ES OTR Oe te eens © a eh Cae Re ee ag
Oe ages ene Rees -s Neck MN Py tee AOR? > oS

BORIS Dre: ee “THE “CAMBRIAN. ee

- comparatively a small number of living forms existing from the period of the final

point.

_. unfolds to us that portion where greater depth and more er condition prevailed. —

el ee” SALE Fhe ma? ne

- development of fossils « occurring ‘at the same point, proves et organic forms to ha ve
flonrished in a littoral position; and beyond these points, where the thinning of the
strata indicates a greater distance from the shore the fossils diminish, and at the mor
distant and deeper points are not found at all. There is no evidence of acuudevell
in these instances, and if there had been the parts left would have retained the same —
_ fossils, had it ever contained them, as they do farther east. . .
Throughout that part of the ancient ocean now occupied by Ohio, fndidon! Michem
~igan, Lllinois, and even to the west of the Mississippi, there appears to have been

deposition of the Helderberg limestones to the commencement of the Carboniferous.
period; while in New York, during the same period, there were a greater number 0:
forms and individuals than in all the preceding periods. Without desiring to dimin-
ish the value of fossil characters as means of identifying strata, it must still be
‘acknowledged that similar conditions in the bed of the ocean, and apparently similar
depth of water, are required to give existence or continuation to a uriform fauna; E
and when we pass beyond the points where these conditions existed iv the ancient
ocean, we lose in the same degree the evidences of ideutity founded upon J fossils, 3
Some species, it is true, have lived onward through successive depositions, often of |
very different nature; yet, at the same time, these may not have had a very wide —
geographical range. In thecase before us, some species have lived during the deposi-
tion of all the rocks from the Hamilton through the Chemung groups, and yet they —
have never extended themselves as far westward as Ohio and Indiana, although the |
nature of the deposits there was as favorable to their existence as in New York, = —

For the distance of 100 or 200 miles from the shores of the present continents the | !
forms may be similar—we know not but they are—still who can say what changes may —
occur, or whether any exist in the depths1,000 miles from land? From the nature of — 3
sedimentary deposits it can be only the finer parts that ever reach to great distances
from their origin; and, reasoning thus, the fauna of the deep and distant parts of
_ the ocean, if any exits would be uniform, not being liable to destruction or change —
of condition from the rapid invasion of variable deposits like those near the shore. aa
The deposition of a coarse sandstone or conglomerate succeeding to ashaly mass would. .
in all probability destroy the greater number of living forms as far as it extended. —
But at the same time, the finer materials produced by the same cause would extend
far beyond the limits of the coarser, and thus approximating in some degree to the = E
lower mass, the fossils might be continued long after they were >» destroyed at another |

One of the most interesting ae in the products on going wentephdil is- nea
great increase of carbonate of lime and the diminution of shaly and sandy matter, © 3
indicating a deeper ocean or greater distance fromland. The source of the caleareons ay
deposits is thus shown to have been in that direction, or in the southwest, while the 4 .
sands and clays had their origin in the east, southeast, and northeast, producing a r:
turbid condition in the waters of these parts during long intervals, which was un- —
favorable to the production of calcareous matter and the formation of chénitost ir
deposits. In New York we are evidently upon the margin of this primeval ocean, as —
indicated in the character of the deposits as well as organic remains; the southwest — i

Ata later date he said : : . te 4

=

La -

I have met with no essay upon the geographical distribution of fossils in the older
rucks; and the few facts here and there gleaned serve rather to stimulate than to sat-_ $
isfy curiosity. It has been a favorite opinion of many, and frequently advanced, that —
the condition of this ancient ocean was uniform and its depth moderate, and that
the uniformity of organic products affords proof of the same. Without peobucataue a 4
to refute any theories or to establish general conclusions for the whole continent or 4
for the whole globe, I shall merely offer a few facts which have fallen under my own |
_ observation, and this with the hope of calling the pipyang® of other pecs to the i

so

By,

Fol © be : <5
cee. As 3 = eae f “2 o: @ : 7 .f F “2AT
oe ~ . q + -

nd. id in deciding pres true cause ‘and adiount of variation in paleozoic char-

8 n all these changes the inflnences of depths of water, distance from or proximity to-
nd, and the influence of the nature of that deposit which formed the bed of the ocean,

* ave influenced the dyloetos character and condition of our older fossiliferous deposits.

i

All these cireumstances a the organic productions of our present ocean, w hat-

_ “this ancient sea, where, dighougi depth and temperature may have been more cra oms;
pare these could not have been paramount to all other influences.!
_ He then proceeds to correlate the strata ofthe Mississippi Basin with
those of the New York section by means of the contained fossils, and
7 Wher possible the order of stratigraphic succession.
Emmons.—In a geological report of the midland counties of North
Pcabetlna; Dr. E. Emmons, in 1856, speaks of the classification of the
2 oe and says in this connection: 3
. Superposition i is, however, the highest proof of age, the oldest occupying the in-
ae Netort position.
eS _ The bearing which fossils have to any scheme of classification which has been
Z proposed can be understood only by a knowledge of the following laws: (1) That
species or kinds have had alimited duration ; (2) that there has been a succession of species;
an and (3) that the species of one period, and which have become extinc:, have never lived in
= any future period. The utility of the knowledge of fossils is based on these three. laws,
_ This knowledge i is particularly useful in comparing rocks which are widely separated
F ae from each other, or in those cases where direct superposition can not be observed. If,
Ee - for example, certain rocks in Canada furnish a group of fossils similar to those of a
¥ given series in Tennessee, the inference would be that they belonged to the same
‘Se period and hence occupy the same geological position; or, if we compare the fos-
e ~ sis of the coal formation of England and Aierica it will be found that they are

Se __almost identical ; and it is proved also that the position relatively is the same in
both countries, (hough separated from each other 3,000 miles. ?

BS 423 Dig extension of the New York section to the south along the line of
Pest the Appalachian Mountains was principally the work of the Rogers
et - Brothers and Prof. Safford.

= Rogers.—As geologists Messrs. H. D. and W. B. Rogers traced the
“the formations by stratigraphic continuity, lithologic characters, serial
relation, and the presence of similar fossils asin the Trenton limestone,
_ ete. [ have not met with a statement of their views of geologic correlation
oF oe "except in incidental remarks. In a reply made to Prof. James Hall,
ao who had congratulated the Profs. Rogers that they had borne such able
ie & evidence to the value of organic remains in determining the age of

ee

__. rock, Prof. W. B. Rogers said :3
BAS: ‘ ‘That they had not been understood on this point; they had followed out the in-
te A tricate structural geology of Pennsylvania and Virginia, relying chiefly on litholog-

in parallel planes to the New York geologists, whose labors among the regular ia

54 ee 1 Nature of the strata and geographical distribution of the organic remains in the older formations of
wae * the United States. Boston Jour. Nat. Hist., vol. 5, 1845, pp. 2, 3.

Share By 2 Geological report of the midland counties of North Carolina. New York and Raleigh, 1856, p. 24.

ae 8A system of classification and nomenclature of the paleozoic rocks of the United States, with an
- = be account of their distribution, more particularly in the Appalachian Mountain Chain. Am,Jour. Sci.,
ES i Yo. tal) 1844, p. 112,

Wie
°.&~
har
us et
ae hy *
ie.
‘a :
rf
|
*.

Se* 4 , a) fe + - y- ih Eee * ~~. ae
s ‘ a = s-.5 ~ - ~ kf TA?

Beer eke _ CORRELATION. a dee 408

‘a when examined over wide districts. We shall doubtless be led eventually to ~

‘i

ise _ ical characters, and had found to their great gratification that they had been working

404, iS Be wide THE CAMBRIAN, | a )
‘ SS - ar if, f

aN horivental Sata of that State, relying on the Svidends of fossil r remains, sind omg 3

- out results in the main quite consistent with the determinations of the Bs i an
Pennsylvania strata. é Sr

In an address before the Association of American Geologists and Nat.

-uralists, Prof. Henry D. Rogers, in speaking of the tracks i in the sand-

stone of the Connecticut Valley, says: ; ; 5 ea 4

Of the organic remains, through an investigation of which alone we can hope to ; wy

establish the position of these stra‘a in the scale of time, or reach definite conclusions — 3a

respecting the physical conditions under which they were produced, the most instruc- - : 3 3

Sa
3
<g -
he
a

4
oe

tive are the remarkable bird’ tracks, brought to light by Prof. Hitchcock, in Con-

hte oe

necticut and Massachusetts. nd
Guided by mere lithological resemblance, Maclure imagined we stratum to be the Og
equivalent of the Old Red Sandstone of England.! a
These passages imply that Prof. Henry D. Rogers ogaeaened pale. : a
ontological evidence of the highest value in correlation, although in his — a
work in Virginia he relied largely upon stratigraphic relations and lithol- e

ogy for the correlation of the Virginia with the Pennsylvania formations.
The correlation of the sandstone beneath the Trenton and Magnesian | .
limestones of Pennsylvania, by Prot. H. D. Rogers and those that suc- —
ceeded him, was based upon the stratigraphic position of the sandstone —
and the presence of Scolithus linearis, a fossil believed to be common to
the Potsdam sandstone of New York and the lower r sandstone of Penn- ©
sylvania. Ks
The evidence of the identity of the sandstone with that of the Pots- a
dam sandstone of New York, on the stratigraphic succession and posi: ‘4 4
tion, is as follows:
(1) The formation is beneath a series of limestones, a portion of which —
is identified with the Trenton limestone by the contained fossils. | 5
_ (2) The sandstone rests unconformably upon the crystalline gneisses E.
‘forming the basal rocks of the Paleozoic period of Pennsylvania. ;
(3) The lithologic characters of the sandstone formation corresponded 4
to that of the Potsdam sandstone of New York. a
The paleontologic evidence is the presence of the annelid borings | “ag
called Scolithus linearis in the band phone ot New York and Foner es
vania. oa

without protest by some of the Sickie in the inition “Mr. @Invilliers? |
calls attention to this corelenon a the pH gas cate in the followin g words: :

in Vol. 1 of this report, it has been called Pardon seietitohe! taking for granted i thaee
any sand formation underneath the Magnesian limestones of the Great Valley noe

[Calciferous ?], finer and other limestones of the Mohawk. Aah

=.

1 On American geology and present condition of geological research in the U nited States. Am. 4
Jour. Sci., vol. 47, 1844, p. 248. 1
* The geology of the South Mountain Belt of Berks County. Second Geol. Surv. of oer Da, vol,
2, 1883, p. 99, f ~ a

~ ¢ : : -

= 2 . C . P w'é4 a ~
5 . a ‘ ’ 7
U 5 Pee -

-_% = >.
4é - . -

if On eo map of Adams County, based upon the results of geological

= . work of Dr. Persifor Frazer, the quartzite resting upon Azoic is iden-
x - tified as Potsdam, with a question mark.

- Safford.—tin his first report upon the geology of Tennessee, Prof. J.
= M. Safford describes the method of the grouping of the Strata into for-

- mations. He says:'
: . _ We often meet with a series of adjacent strata similar in many respects, so much_
oe so that they can conveniently be thrown together in a single group or formation, as

~

rn such a series is often termed.
He says further:

For example, the sandstone, slates, and coal which form the upper part of the Cum-
- berland Vable-land, are grouped in a formation, called the Coal Me: asures, with the fol-
lowing among other common characters: First, coal is found at intervals throughout
ey the series ; secondly, there is very little limestone or calcareous matter in the series: :
oi thirdly, the strata are parallel, and appear to have been formed in succession, under
te ‘similar circumstances; fourth/y, the same fossils, such as different species of petri-
- fied shells, leaves, branches, and trunks of trees, etc., occur imbedded in the rocks
~ throughout the length and breadth of the series. Characters similar to these unite
the strata of all the-formations.
The character last mentioned we must refer to more particularly, on account of its
great importance in designating with precision the group to which local and isolated
_ beds of rock belong.

In defining the use of fossils it is stated that each formation has, in
_ great part, its own fossils.

Most of those found in one do not occur in any other. Upon this fact depends their
great utility. They furnish, when known well enough to be recognized, unmistak.
~ able evidence of the geological position, and hence the general character of the for-

: mation in which they are found.

hee

+

‘ of correlation which he used, as follows:

I. Stratigraphic position.
II. The oceurrence of similar fossils.
Ill, Lithologic characters.

CANADA,

¢
~ ve *
’ $

Peles

‘The New York series was traced into Canada by Sir Wm. E. Logan

ne and his associates and correiations made by direct stratigraphic conuec-
tion, and in the absence of that, paleontologic data, stratigraphic rela-

va Goa and lithologic characters.

4 _Logan.—In speaking of the stratigraphic succession of the New York
“and Canadian sections Sir W. E. Logan makes the following reference

. to the fossiliferous limestone above the Calciferous sandrock, or the —

t- Trenton limestone:

: _. The lowest of the fossiliferous strata is a sandstone of variable quality, more purely

siliceous towards the bottom, and calciferous towards the top, which gives support
be to a thick and remarkably pareistelt deposit of limestone, strongly distinguished by
- its organic remains. This limestone thus becomes an admirable means of tracing

5) LSE ee ee ee

we ls *
oa a

te eee JA geological reconnaissance of Tennessee ; first biennial report, Nashville, 1856, pp. 130, 131.

x
—
3
wa
os

oa ba “pil i ‘ : -
Su NG a
Ox: ty -* 4
oo Ss," 5

id ene ee ay a we Pn OO ee PL oy Se Ae h) &-

sitet CORRELATION. Fe 405 -

From these observations of Prof. Safford we postulate the principles —

one - ge te Be ee ES ale a or ome ote ee oe
' Wes a <! ey ~*~ y. 4 a iy >
Aes, ‘e . .s

ADB oS Soy tT CAMBER SE 2 a 20" mat gles!

out the Garinoter of the ereat western area endex’ aden nies “Wrote tha. north- : <=
west border of North Carolina it sweeps in a broad belt across Virginia to the junc-
tion of the Shenandoah and Potomac. Thence traversing Maryland, ‘it passes 2

through Pennsylvania by Harrisburg, on the Susquehanna, and Belvidere, onthe |
Delaware,accompanied up to this point by the underlying sandstone. Diminishedin
its thickness, it thence crosses New Jersey, and reaching Poughkeepsie it passes up j
the valley of the Hudson and Champlain, keeping to the east of the river and the - 2 :
lake, and attains the neighborhood of Missisquoi Bay. Entering Canada, it pro-_
égeite towards Quebec, and it reaches the vicinity of that fortress ; ; but lam not yet
aware of the precise spots at which it is visible in its course shithars farther than 4 *
that I have been informed a stratified limestone answering its condition is quarried —
and burned in the Seignory of St: Hyacinthe, east of the Yamaska River." SS

_

He states that the city of Quebec does not stand on this — pincer 4
but it is found below the city on the north shore of Beauport and —
farther down the river to Cape Tourment. Following up the valley of _
the St. Lawrence, it is found to run along the foot of a range of syen-
itic hills, and it leaves the river in the vicinity of Montreal and again ~
appears in the Ottawa Basin. He then describes its extension south |
along the valley of Lake Champlain, and west through the valley of
the Mohawk and Black River and north of Lakes Ontario, Huron, and} B.
Michigan, to Wisconsin, following thus the correlation made by Hall. 4

NEWFOUNDLAND.

The extension of the Canadian nomenclature to Newfoundland was
the work of Messrs. Logan and Billings. In tracing the Paleozoic for.
mations down the St. Lawrence River from Montreal, Logan found that
a series of sandstones occurs beneath the Calciferous sandrock, which —
was well recognized beneath the Trenton limestone. The sandstones —
rested unconformably upon the subjacent Archean. A long joer Py
exists between these exposures and those on the north side of the =
Straits of Belle Isle, where sandstones and limestones are superjacent —
to the Archean. In his first expression of opinion he calls the sand-
stones the Potsdam, from their stratigraphic position and lithologic —
character. When the fossils which were obtained from the associated
limestones were examined by Mr. Billings and found to be ‘identical —
-with those that he had referred to the Lower Potsdam in Vermont, the
strata on the north side of the Straits of Belle Isle were referred with.
out reserve to the Potsdam horizon, and those occupying a similiar
position on the west of Newfoundland were also similarly referred?

When correlating the Lower Cambrian sandstones and slates of
northern Vermont with the limestones and sandstones of the north _ ;
shore of the Straits of Belle Isle, upon the lithologice and paleontologic —
similarities between the two deposits, Mr. E. Billings states that although 4
860 miles distant from each other there can be little doubt that— ‘they
are of the same age. rs ye ee

: ee = = jee

1[Account of general structure of an extended area in North America.] Geol. Survey Canada, Re a
port of Progress for 1843, 1845, p. 8. ‘
2 Geological Survey of Canada; Report of Progress from its commencement to 1863, PP. 97 2 7
289, 864, 865. Montreal, 1863. ; ie 2

“othe: occurrence of Scolithus linearis and the eee aspect of the fossils also show

ho
-
_

A - with the Upper Primal sandstones and slates of Pennsylvania.!

e. The Lower Paleozoic rocks of Newfoundland were correlated with
_ those of Canada by Sir W. E. Logan upon the evidence of the fossils
and their stratigraphic position.. The fossils were identified by Mr.
“Billings, and the stratigraphic geology was studied by Messrs. Richard-
* ae iad Murray, and Howley.

- Dana.—Prof. J. D. Dana availed himself of the correlations made by
“the New York, Canadian, and other surveys in the preparation of the
earlier editions of his Manual of Geology. The Manual is a masterly
_ compilation of the available data upon broad principles of correlation,
_ and as it went at once into the hands of all American geologists and
_ students its influence has been widespread. The principles of correla-
_ tion mentioned are outlined in the following paragraphs:
fe But the question may arise whether a_ geological age is not, after all, strongly
~ marked off in the rocks. Rocks are but the moving sands or the accumulations of

dead relics of the age they represent, and are local phenomena, as already explained.
‘Each continent has its special history as regards rock-making, and it is only through

_ the fossils in the rocks that the special histories are combined into a general system. .

- Movements have in all ages disturbed one hemisphere without affecting the other,
near breaks in the succession of rocks in one continent or part of a continent that
- have no representatives in another. .

When an age can be proved, through careful study, to have been closed by a catas-

er

~ trophe or a transition which was universal in its effects, the event is accepted as a

grand and striking one in geological history. But the proof og be obtained
- before the universality is assumed. Hence the conclusion:
Fourthly. The grander subdivisions or ages in geological history based on organic
_ progress should be laid down independently of the rocks. They are universal ideas
for the globe. The rocks are to be divided off as nearly as practicable in accordance
z with them.

- Each eontinent, under these ages, then becomes a special study, and its history has

es periods and epochs which may or may not correspond in their limits with those of
- the other continents. Every transition in the strata, as from limestone to sandstone,
clay beds or conglomerate, or from either one to the other, and especially where there
’ is also a striking change in the organic remains, indicates a transition in the era from
one set of circumstances to another; it may be a change from one level to another in
the continents, a submergence or emergence or some other kind of catastrophe. All

i such transitions mark great events in the history of the continent, and thus divide

_ the era into periods, Sasa periods into epochs, and epochs, it may be, into subepochs.
Hence— .
_ Fifthly. Through the ages each continent had its special history ; and the periods
- and epochs in that history are indicated by changes or transitions in the rock forma-
tions and their fossils.
It is greatly tothe assistance of research that some of the revolutions of the glube
s have probably been nearly or quite universal. The one preceding the Mammalian
_ age appears to be an example; although, even with regard to this, further investiga-
_ tion is required before its actual universality can be regarded as established. But
_ the periods and epochs of America and Europe are not in general the same in their

- "Paleozoic fossils. Containing descriptions and figures of new or little known species of organic
_ remains from the Silurian rocks. Vol. 1, 1860-1865, p.2. Montreal, 1865. First printed in 1861 in a
= bulletin issued ae the Geological Survey of Canada.

@ORRELATION. = pee! i

that these rocks must be very nearly, if not exactly, in the same geological horizon

-

- parallelism between the periods and epochs marked off on each continent, and —

te RO OSE BS eS A Fe tt ging Fees a a Ee a ee) ree wee ‘CR a en
nate Rares aa he ays ORS Core Make
+> < = Meh (~< o a op Ne Po os Ye RS > Rd
- = ‘ - a,” ee ey Ae wos
fe ae hs +e EEE Se pRB i DE BS Lh 8 .
ett Me Yee > MB a ee taal ee he ok aE Sy he
»2 - ] =H% - ’ J : “ 7 Ay a tok ar OF 9 =
5 y Sa Le tet. te ’
ALS -- I sane a : © - oO os
408 “THE CAMBRIAN, = Recent

oe . ce

limits. A near contemporaneity in rocks may be proved, but a in the transitions
from one rock to another. For example, the Devonian age has a very different series
of periods and epochs in North America from what it has in Europe, and there is.
even considerable diversity between the epochs of New York and the Atlantic ane ,
and those of the Mississippi Valley. The Carboniferous, Reptilian, and Mammalian _ Ca
ages also have their American epochs and their European, differing from one another; wy
and the differences between the continents increase as we come down to more modern | j
times. There are Tertiary and Cretaceous rocks in America as. well as Europe, but :
there is little reason for the assumption that the transitions from one set of Tertiary —
or Cretaceous strata to another were, in the two, contemporaneous. The ae should
be proved, not assumed. We add, therefore, | ee 2

Sizthly. Itis an important object in geology to ascertain as nearly as possible the | 3

study out the precise equivalents of the rocks, each for each, that all the spacial ss
histories may read as parts of one general Supe? and thus Consbean to the per-— a q
fection of one geological system.! \ <A

MISSISSIPPI VALLEY. ‘ . -

The Lower Paleozoic rocks of this region were correlated with those — %
of New York by Messrs. Owen, Locke, Hall, and others, usually with--
out stating the data except by implication (e. g., speaking of the Tren-
ton limestone of New York as a limestone carrying certain fossils and —
superjacent to a marked formation, the Calciferous sandrock of New ‘
_ York or the Lower Magnesian limestone of Wisconsin, ete). Thus the Ee

correlation is based upon stratigraphic poNriOn, presence of similar
fossils, and lithologic characters. : BS 2
- Hall.—The following observations by Prof. Hall are a good. illustra.
tion of the method by which the Potsdam sandstone of New York was
correlated with the lower sandstone of the Mississippi Valley section: a “ .

~

+y

_ In comparing the older rocks of New York and of the East generally with those Pe
the West it should not be forgotten that there is a long interval on the line of the ‘2 2
northern outcrop of these ancient strata between the St. Lawrence and the western | B,
limit of Michigan on the Menomonee River, where we can expect little aid from pale-
ontology. The fossiliferous beds of these ancient formations in Wisconsin lieto the
west of what appears to have been a great promontory at the time of their deposi- —
tion, stretching southward from the region of Lake Superior far into the ancient sea.
The disconnection caused by this promontory between the East and the West would © S
of itself prepare us to expect a fauna differing in a great degree from beds of corre-- .
sponding age on the opposite sides. oe
_It has been shown by the investigations of the Canadian Survey that not only the > .
_. Potsdam sandstone but all the fossiliferous beds below the Birdseye and Black River
limestones are absent from Kingston, on Lake Ontario, to Lacloche, on lake Huron. ~
From Lacloche to Lake Superior there is a sandstone coming in below the Birdecteay
limestone, which, from its position, may be considered as of the age of the Chazy* for- —

: Mitta of Geology, 1st ed., New Haven, 1863, pp. 126-128. ; _ a 7
2Preliminary notice of the fauna of the Potsdam sandstone, with remarks on the previously known
species of fossils and descriptions of some new ones from the sandstone of the VER Mississippi Val- sf
ley. 16th Ann. Rep. Reg. State Cab., Nat. Hist. N. Y., 1863, pp. 211-213. ee:
3 The ‘ Chazy formation’ of the Canadian Geological Si vey, in its eastern localities incldiies a sand.
stone which comes in below the greater part of the limestone, leaving from 10 to 20 feet of shale and, lime- ho:
stone beneath (Geology of Canada, 1863, p.123). It is apparently this sandstone of the Chazy forma- 4 ;
tion. having in Canada a thickness of 50 feet, which has become augmented in its ig hte extension —
while the calcareous part of the formation has partially or entirely disappeared, + TR a alta Bae
wit mag

é eee. sf iz

“
— > 2) te « = 5 “4 , 4 rigs
SS . ? ‘¢. _ aN o

o. Bee Scie ee EI OP ee Ee ee eae
« - > 7, ~ i > a= er ot > a ae iy
ef, ~

ert ee + WH sry ~ rs a

Sheet a

Ss

2
tome localities along that line.
ne 2c Phe, succeeding Birdseye and Black River formation from Lacloche to Lake Supe-

« se" Se cwectone, doubtless, whieh é been taken on the Potsdam sandstone in

oh
aa color, but still holding the characteristic fossils. ;
nos - In New York a sandstone (the Potsdam) lies immediately beneath a magnesian
~ limestone (the *‘Calciferous sandrock”); this deposit is succeeded by a calcareous
formation (the Chazy), including a sandstone and surmounted by the Birdseye, Black
> Biv and Trenton limestones.
In Wisconsin, Iowa, and Minnesota we have undoubted Trenton limestone, and

“*s Poe

: £ tie fossils of the Birdseye and Black River limestones as to leave no doubt of the

26 para allelism of these beds with those of New York. Below this magnesian limestone

RSS we e have the St. Peters sandstone, corresponding, as already shown, with the Chazy

= ological character, corresponds in all respects with the ‘‘ Calciferous sandrock” of New
| York, . ate,

‘ ~ It is from all these facts that the lower sandstone of the Upper Mississippi Valley

; oS Sen? oe CORRELATION. ~ | = 409°

below it a buff-colored magnesian limestone containing so many of the characteris-

ee rior has become a buff-colored magnesian limestone, or weathering externally tothis —

nt ‘se mation, and beneath this a magnesian limestone, which, in its position and lith- —

a> ais been placed i in Parelolicn with the sandstone of New York known as the “ Pots- -

dam. i

i Notwithstanding, however, that this sequence is precisely like that observed in

New York it may not yet be regarded as proved that the sandstone from which I

a have described these fossils is in all respects the equivalent of the Potsdam sand-

Ht stone of New York, Vermont, and Canada. It may represent more or it may repre-

is sent less than that formation. The lower accessible beds of the Mississippi Valley
_ May represent the Potsdam of 150 or 200 feet in thickness in the typical localities in

&
ot - New York, while the middle and upper. beds of the West-may be of epochs not repre-

sented in that part of the series studied in New York ; and in some other places, as —
-- in the regions just mentioned, the same epochs may ‘bn represented by a shaly or

oBeiui-culvaveons deposition, or may be included in the commencement of the Calcifer-

ous epoch. It should not therefore be regarded as decided that the Potsdam sand-

e stone, as developed in New York, occupies the entire interval from the base of the

~ oldest sedimentary formation of the Paleozoic era to the Calciferous sandstone, From

Bony what we know of the Primordial fauna in other localities -we are prepared to find

ie. beds above or below, or both above and below, the epoch represented (so far as now
-. known) by the Potsdam sandstone of New York, and which may still be of the same
period.

= Winchell.—It is stated by Prof, N. H. Winchell that—
Bere It has been abundantly proved that the red sandstones of Lake Superior, however
*

in disturbed and changed locally, or however much increased in thickness by the agency
oa of yoleanic outbursts, are the exact equivalents of the New York Potsdam. They

i ~ they lie unconformably, and from which they differ in being but slightly and only
33m locally metamorphosed. They retain usually their evidently sedimentary characters,
jand have not well preserved fossil remains.!

re He also publishes a table showing the number of species common to
b ade Silurian formations of the Lake Superior district and New York
¥ ‘State, and calls attention to the fact that three species only are found
ia in ‘the Lake Superior sandstone and the typical Potsdam sandstone of
_ New York.

o \

a sketch of the geology of Minnesota. Geol.and Nat. Hist.Survey, Minnesota, Ist Ann,
p. for 1872, 1873, p. shes

"occupy the first position over the metamorphic slates of the Huronian rocks on which.

. a4 4a5 a, = noe iG.
=< + - 7 = oe 5 ‘; a: * Songr® = ae Fass <a = oe ee
- E Sis) FSS SRS eee
5 > — — _ vie) eS > te “eae re
. > - ey a hs mw DX i Z < g
| ~ . So Dy Ee ee
410 pe: CAMBRTAN. 22 2 = Be
: . ar da iat ceo

; The correlation by Prof. N. H. Winchell of thie: a Granular Quartz : oa
_ and the “ Red sandrock” of Vermont with the “ Potsdam ” ines

of the Upper Mississippi Valley and the “ Primordial ” quartzite of the -
Northwest appears to be based upon the fact that the “Granular fe
- Quartz” of Vermont and Massachusetts rests unconformably upon the |
Archean, and that a similar quartzite is superjacent to Archean rocks —
in the Mississippi Valley. This same principle of correlation appears —
in his statement that the stratigraphic relations of the “ Granular —
Quartz” and the Potsdam of New York are the same. He says: “In
the first place, they are seen to lie unconformably upon the older gran-
ite.” ! : e% Le

Messrs. N. H. Winchell and H. V. Winchell correlated the Winooski zs %
- marble series of Vermont with the Stoekbridge limestone (or marble _
belt of the southwestern portions of the State.”

This correlation is based upon (a) the assumed “Primordial age of uo
_iron-bearing limestones and shales of the Penokee-Gogebic range of — »
- Wisconsin and the Mesabi range of Minnesota, and their assumed strat- _
igraphic identity with the limestones and shales of western Vermont, — ze:
which correspond to the Stockbridge limestones and iron ores of west- og
ern New England ; (0) the known Cambrian age of the Winooski marble 33
series. Vonks

Meek.—As paleontologist of the Hayden and other surveys of. ei
interior and western continental area, Mr. F. B. Meek’s influence upon
the correlation of fossiliferous strata was important. His views upon
correlation by paleontologic evidence are given in a report on the Pale >
ontology of eastern Nebraska, as follows: * "ae

-
a

oer
=

There are probably few well informed geologists who will at the present time
maintain that the occurrence of a very similar or even the same group of fossils at
widely separated localities necessarily proves the rocks in which they are found to :-
be of exactly contemporaneous origin. The most that is now generally maintained |

in this regard is that such identity or correspondence of types at very distantly —
Fraarate parts of the world indicates that the strata in which they are imbedded
were formed during the prevalence of identical or similar physica] conditions at
_- some time during the same great geological epoch, and that they hold the same “Or 4
nearly the same relative position in the geological column of theirrespective districts, —
For instance, although a stratum in the Rocky Mountains, containing the remains of
very nearly the same fauna as some particular suldivision of the Devonian system i
of Europe, might, for aught we know, be hundreds of years older or newer than that. - Ke
particular division, we would have little or no room for doubting that it belonged to |
- the great Devonian series, or possibly even to some definite, known horizon in ‘ae >
series. We could moreover very positively assert in such a case that it would be, = —
according to all past experience, useless to seek there at any lower geological hori- — .
zon for workable beds of coal, or to expect to find Silurian rocks or any of their pe-

1 The crystalline rocks of Minnesota. General report of progress made in the study of their field — =.
relations. . Statement of problems yet to be solved. Geol. and N. at. Hist. Survey of Minn., 17 th my -
Rep. for 1888, 1889, p. 49. -

? The Taconic Iron Ores of Minnesota and Western New England. Am. Geologist, vol. 6, 1890, pp.
263-274.

3 Report on the Paleontology of eastern Nebraska, in Final Rep. of U. S. Geol. Shay: of Nebra a
Washington, 1872, p. 83. ° ; Site 3) eee

_—. +o
4 : = oa RS. Pigs *dhae-,

= ay eT ee awe) See eee Se OF Eee A a ee eee Oe eee
F 4 See et oe or wt Pe —-_ a 9 ye e - < > —_ tes ‘.¢ -
Set Pe e Nap at Nery ee ‘ AEG

L_- ey: M.S - a" sr - é .

~ .> “y 2 < . 7

|. 3 Siete Be CORRELATION. a All

“ e =

lis Tr orc rod iabots. above, Pits i ised had been no overturning of the strata ‘at the
arti ular localities.
on ace e, palthough Paleontology does not enable t us to gacertain the exact actual ages

4 eonsi¢ sable precision. It is therefore not eho one of the more nnekGhit aids to
* Piha geologist i in his investigations, but in the present state of geological science it
@ ‘Se is the only sure guide in classifying and determining the order of succession of rocks
| where this can not be done by their actual continuity or obvious superposition. For
_t ese reasons it is now the universal practice in all geological surveys conducted
Fe: “upon sound scientific principles to devote especial attention to this department.

Ee peo mt.

ect Sh SES ee ROCKY MOUNTAINS.

2” Me eae es 7

ye OS Wahiiney. he ARS of the occurrence of the Primordial fauna in
evade Prof. J. D. Wifitney calls attention to the fact that the fossils
; are of Potsdam age, and that similar trilobites and brachiopods oceur
Be ~ in Bohemia i in argillaceous shales; throughout the United States, from
- New York to the Rocky Sitchin’, in the * Potsdam sandstone, or in
the shales or slates ;” in Texas and in Nevada, in limestone. He says:
This discovery will also indicate the necessity of caution in theorizing on the geo-
- togical structure and age of regions which have only been hastily examined. It will
~ not do to put down every red-sandstone group below the Trias in the far west as -

pose &6 Potsdam,’ ” for that subdivision may be much lower down, hiding itself as a modest
4 - Timestone « of a very neutral tint of color.!
4 Tem Although not stated, it is evident that the principle of correlation
2 used i is purely biologic, or the occurrence of similar fossil remains.
= - Bradley. —When describing the strata upon the western base of the
S Wasatch range, near Ogden, Utah, Prof. F. H. Bradley refers the
_ quartzite, some 1,500 feet in Uhiskaieen, to the Potsdam, and the gray and
_ calcareous: shales.and limestones above to the Binet and Lower Silu-
~ rian. 2 A reference to the Upper Silurian was on the assumption that
the limestone was the same limestone as that found 25 miles to the
north, in which the characteristic Niagara coral Halysites catenulata was
obtained by Dr. Haydenin 1871. The data upon which the other cor-
relations are made are not given. Itis probable and almost certain
that the presence of a quartzite beneath the limestone, supposed to be
F< aft Silurian age, was considered to be sufficient for the reference to the
Potsdam sandstone. He correlates the glauconite sandstone beneath
Be limestone of the Teton range section, which carries Conocoryphe
4 a and Dikelocephalus, with the Knox sandstone of Safford, in Tennessee.
Br Beneath them, and often present when they are absent, he found from-
sla 15 feet of a very compact ferruginous quartzite “‘ which must rep-
resent the shi cea

*

9

§

q

ote on the occurrence of the ‘* Primordial Fauna” in Nevada. Am. Jour. Sci., 3d ser., vol. 3, 1872,

>, >

2 Ri bof Frank H. Bradley, geologist of the Snake whine Division. U.S. Geol. Sur. of the Terr., 6th

-

ATE 2 Sacer t oie ae CAMBRIAN.

It is evident that Prof. Bradley had in mind the Tennessee section,
with which he was familiar, and on finding a quartzite, correspond. —
ing to the Chilhowee quartzite, and then a sandstone and shale corre-
sponding in position to those of the Knox section, he correlated the two 7
upon the evidence of serial relation of similar iaeate and the presence |
of certain fossils in the limestone superjacent to the sandstone, — m

Fortieth parallel survey.—The correlations made by the fortieth paral-_ ‘#
lel survey of the Paleozoic rocks of Utah and Nevada with those of the
eastern part of the continent, especially the New York section, are B
based almost entirely upon the paleontologic evidence as determined %
by Messrs. Hall and Whitfield. Within the area of the survey corre- |
lations were made both on the stratigraphic succession of beds of dif.
ferent lithologic character, and the presence of similar organic remains.
A correlation based on the “likeness of two great masses of rock to —
each other that occur beneath a known horizon” is made by Mr. Clar-
ence King as follows: ,

Comparing the quartzites and argillites with those of the ‘Cambrian section in *:
Wales, the likeness is too great to pass unnoticed, and in view of the enormous de- —
velopments of these low-lying rocks as compared with the Silurian lying above the |
Primordial horizon, I have determined to draw a line at the upper iimits of the Pri- —
mordial period toinclude the uppermost members of the’Potsdam epoch, and to con- —
sider the whole underlying conformable series as Cambrian down to the point of ~
‘their nonconformity with the Archean.' ;

Explorations and surveys west of the one hundredth meridiak-Tie
correlations made in the publications of this survey on the Lower Paleo- —
zoic rocks are mainly by Mr. G. K. Gilbert in his report on the geology —
of portions of Nevada, Utah, California, and Arizona.? The dataused _
for correlation are, the stratigraphic position, lithologic characters,and _
the presence of fossils of previously determined range.- No attempt is
made to correlate by a study of the minor details of the faunas and —
strata except in the correlation of the Tonto of the Grand Cajfion dis- —
trict with the Primordial formations of the East. From the known
position of the genus Cruziana he argues that the beds containing it i
are Lower Silurian or Primordial. Mr. F. B.Meek compares the species _
of Olenellus found in central Nevada with 0. thompsoni and O. vermon-— a
tana of Vermont and thus indirectly correlates the faunas.? i

Geological. surveys of the Territories.—The correlations made by the
various writers of the Powell and Hayden surveys were principally =
based upon the paleontologic determinations of» Mr. F. B. Meek and —
Dr. C. A. White outside the territory of the survey, and within its ter- ;
-ritory on stratigraphic positions, lithologic character, and fossils when
present. In most instances the data for correlation are not given, the “3
identification of the formations following that of previous workers in |
the same territory. An example of this is found in the “ Geology of the ©

»

_ 1 Paleozoic subdivisions on the 40th Parallel. Am. Jour. Sci., 3d ser., vol, 11, 1876, om 476, rl
? Expl. and Surv. West of 100th Merid., vol. 3, 1875, pp. 156-171. i=
3 Op. cit., pp. 182, 183. : :

iD. Ss. Geological Survey.—In the Honschidaltoa of the various Goy-
? - ernment surveys and their reorganization under one head in 1879 the
@ _ opportunity for broad comparisons and studies was increased, and the
eet mitios were still further increased in 1881, when the survey was
extended to include the entire areajof the United ‘Biatee: In the Rocky
Mountain Province the correlations of the fortieth parallel survey
E _ were accepted, and extended in the abstract of the report on the geol-
_ ogy of the Bureka district of Nevada.' In the report on the paleontology
ese of. the district the paleontologic data upon which the correlations were
= made are assembled and described.? In this it is shown that while corre-
E lations between the great groups may be extended between the Appa-

lachian Province and the Rocky Mountain area, it is impossible to
a correlate the minor divisions of the groups.

__ In 1886 an extended correlation of the rocks and fossils from the
2 _ Lower Cambrian, then called Middle Cambrian, was published in Bul-
x letin Nd. 30 of the U. S. Geological Survey. Typical sections are
x & - given of the Cambrian rocks of the Atlantic Coast, Appalachian, and

Rocky Mountain Provinces, with the names of the species of fossils

Pe occurring in the various zones, and on page 44 the various sections are
correlated and grouped in a table to show their relative range. The

_ principles of correlation are not enunciated, but those used, as shown

& Sty the text, are the stratigraphic position of the faunas in ERS to
E each other in the same province and a comparison of the faunas in one
3 area with those of another.

Ina more recent work‘ the correlations are made between the various
horizons of the Cambrian of the United States on the stratigraphic
position of the strata and the occurrence of similar groupings of organic
remains. It is observed that the presence of the Olenellus fauna is

= regarded as the strongest factor in the correlation of the Lower Cam-
_ brian, and it is assumed that the presence of this fauna indicates the

_ same geologic horizon. It is not implied that the formations charac-

terized by the Olenellus fauna are strictly contemporaneous wherever
i. has been found. On the contrary, its presence in such widely sepa-

rated localities as England, France, Spain, Nevada, and British Colum-

dia is considered as prima facie evidence that the deposits are not
a ‘Strictly contemporaneous. That they were contemporaneous in a geo-
3 eee senseor that they occupy the same relative position in the geologic
_ Series is accepted throughout the paper.

ay

& 1 Third Ann. Rept. U.S. Geol. Survey, 1883, pp. 248-272.

- 2Mong. U.S. Geol. Survey, vol. 8, 1884.
hs 8 Walcott, C. D.: Second contribution to the studies of the Cambrian faunas of North America.
. ‘Sorin
4Walcott, C.D.: The fauna of the Lower Cambrian or Olenellus zone, Tenth Ann. Rept. U.S. Geol,
Survey 1890, pp. Bios

Be EP RO PISA ee ine PINS ae Eee a ae aan ae ey
eee eee i POA Sec rk pe NS
414 — “THE CAMBI io ie
ie THE eer eee

In his extended and ‘valuable essays upon fin tio: of the ae
Cambrian and Silurian in geology and the Taconic question i in geology Vy -
and numerous other minor papers, Dr. T. 8. Haunt! clearly sets forth a
the description of the various strata referred to the © Cambrian and — <4
Silurian in America and Europe, and shows by testimony of different
writers the relations the various formations sustain to each other, both 7
stratigraphically and in their geographic distribution. Nearly aus i s
not all, the original correlations made by him are based upon lithologic ©
data, as he believes in a uniform development and sequence of litho. | .
logic forms from earlier Archean time to the deposition of the fossilif. _
erous sedimentary rocks. Thecorrelations within the latter are largely
made upon their stratigraphic, lithologic, and paleontologic characters _ :

as mentioned by authors. 7 Mae 5 a

CORRELATIONS WITH EUROPEAN FORMATIONS. ct

Numerous correlations were made between the strata of the forma- 3
tions of America and those of Europe by Messrs. Conrad, Owen, Rogers, —
Troost, Jackson, and others; but it was not until the investigation of. |
M. Edward de Verneuil, in 1847, that correlations were made by one
who had personally Sipuatipaeat the formations and fossils, both in
Europe and America.? a

De Verneuil.—He began his comparisons with the view that super: 3
position was the foundation of paleontology; that the only compari-—
sons that could be made between continents separated by a sea was
by a study, in each of them, of a series of beds confined between two -
zones at well determined points; that their fossils must be compared, |
and the identical species picked out to see if the species are distributed
according to the same laws. He concluded that, if it happens” in the
two countries that a certain number of s) stems, cnaractariagl by the
same fossils, are superimposed in the same order, whatever may ‘be |
otherwise their thickness and the number of physical groups of. which _
they are composed, it is philosophical to consider these systems as
parallel and synchronous. Comparisons were made between the strata -
in the two countries that occur beneath the coal-bearing or Carbonifer- |
ous rocks. He noted that the Potsdam sandstone with Lingulais prob-
ably analogous to the sandstone with Obolus, of Russia, and the lower |
sandstones of Scandinavia. ‘These are in the two continents the |
most ancient pre-Carboniferous rocks.” ee

The siliceous limestones, those of Black River and of Trenton, are the equivalents"

of a great part of the Lower Silurian stage of Europe, and pee. occupy the same Lene?
o se *

-

' History of the names Cambrian and Silurian in Geology. Canadian Nat., new ser., vol. 6, 1872, 1 pp.
281-312, 417-448. The Taconic Question in Geology. Mineral Physiology and Ph ysiography. ge
ond series of Chemical and Geological Essays. 1886, pp. 517-686.

2Note sur le parallélismé des roches des dépéts paléozoiques de |’ Amérique Soptepantaieeue avee
ceux de l'Europe, suivie d’un tableau des espéces fossiles communes aux deux continents, avec Vind
cation des étages ow elles se rencontrent, et terminée par un examen critique de chacune de ces espéces.
Soc. géol. France, Bull., 2° sér.,vol. 4, pp. 646-709, 1847. Translated and condensed by Prof. J rein Hall.
Am. Jour, Sei., 2d ser,, valk 5, 1848, pp. 176-183, 359-370; vol. 7, 1249, pp- 45-61, 218-231, eae

ae
Pe
“ag
i +

SaaS Not gS Sohege a ye he AY ah on Pee Pe Ne Hl ay Eee ete Wes
3 As > = fe ORE ty sie co. a <7 eS “i lt = a oi > 4 2 4 Tor.
LAO ete WF rad k*. >, £ 2 we Pes
Beane ke - CORRELATION. Pe ae oe A15 in
- s 4 ; : : , c

4
\ “-

base, Ceateaertt the Graptolite slates which in Sweden Raskaoe to the red Orthocera-
pary 7 “tite limestone. They are also the same as those of Bain in France.!

Of the Upper Silurian rocks the Niagara group is considered the
a ead equivalent of the limestones and slates of Wenlock and of Goth-
se land. The Clinton group, with Pentamerus oblongus, represents the
re extreme upper part of the Caradoc sandstone, or a stage intermediate

>.

: ae between the Wenlock and Caradoc beds; while the five inferior
Rio groups of the Helderberg division represent the rocks of Ludlow. The
RS correlation is then extended to the Devonian, and lists are given of
identical species of fossils ou the two vontinents.

_ Hall.—The essay of M. de Verneuil was followed in 1851 by a paper

Se ferina ‘“‘ Parallelism of the Paleozoic deposit of the United States and

Gere

Europe,” by Prof. James Hall. In ipa cera the criteria of correlation

he says:?

The simplest principles of elementary geology teach us that sedimentary beds, hav-
_ ing the same thickness and the same lithological characters, can not have spread
over an area so wide as that now included between the European and American con-

+o
. -
ad

‘“

-

- tinents. All sedimentary deposits must vary in character at remote points, as the —

ae oa - physical conditions of the ocean can not be presumed to have remained the same over
__ awide extent of surface. Under such circumstances absolute parallelism is not to

, be sought for orexpected. Calcareous deposits, as would naturally be supposed, have

_ been found to be more persistent and more uniform in the character of their fossil con.
e tents; but these, over some portion of their extent, have often been invaded by
a argillaceous and arenaceous sediments, and the fauna is found to be in a greater or
fe less degree influenced by such circumstances. In distant and disconnected localities
ioe we are compelled to base our opinions of the equivalency of beds upou the organic re-

Foe ‘mains which they contain ; and when we reflect that the nature of the sediment may
z ‘in agreat degree buinened the character of the fossils we shall not fail to recognize
aa the necessity of keeping the character of these lithological changes in view. * * *
_ Besides the changes which take place in the nature of the sediment deposited upon
_ the bed of the ocean, we are to look to other important conditions which may affect
ek the fauna, and consequently our conclusions regarding the equivalency of forma-
ae tions. Among the most important of these is the depth of the ocean in which the
ne animals lived, since we know that certain species are confined within certain zones,
aS depending on the depth of the water.
ae There are other conditions which sensibly affect the distribution of organic life,
7 such: as temperature, pressure, and light. * * * In investigating the fauna of
past ages we see nothing to lead us to believe that the same great laws which regu-
“tate the distribution of species did not then operate with as great effect as at the

oe time,
ves Ee speaking of the attempted correlation between the European and
ae +

"American rocks Prof. Hall remarks:

: Dn All the attempts to show that the parallelism of American and European paleozoic
deposits have been with a view to find a correspondence with the European stand-
ara where the scries is confessedly incomplete, and where it has suffered during its

oe deposition, or subsequent to it, many disturbances.*
ee -

os 1 0p. cit., p. 361. *

‘a Pubs __ *Report on the Geology of the Lake Superior Land District, by J. W. Foster and J. D, Whitney;

= Part 1, 1851, pp. 286, 287.

> has cit., p. 294,

s

wt—e, > af “2a 2 t ~ty ™~ tt w. i, ee eS @
Se SC Pe ET age Soe ga Ne he eee POE

Ss = =f) = eis wt. ‘. 7 x s. ri ter f 6 Teer 33 me. ee et ee
ot ale ve é 4 - = ) \ - = = -e & > a eth s> < 26 ES i

6 : te ‘s ate Sx 36) ;
sc es ; (3s oo TRE ‘CAMBRIAN. ” Na Sol hal eg ee

‘The author agrees with, M. de Vernenil that the » Potsdam sandstone i is YS oa

in Seandinavia by the sandstones which rest tnneitoemanle: upon the |
gneissoid and schistose rocks composing the Azoic system. Of the x
Chazy, Birdseye and Black River limestones of New York he ‘says:

They are not very clearly recognized in Europe. It is probable that some part ee
the Orthoceratite limestone of Sweden is the equivalent of the Black River ass 5 “s ¥
but we have no evidence, from fossils or otherwise, that there are any representa: ;
tives of the two lower rocks. * * * “

The Trenton limestone, the Utica slate, and the Hudson River _group are repre-_ %
sented in northern Europe by the Orthoceratite limestone of Sweden and Russia and .
by the shales with Graptolites, which succeed to that limestone, In Great Bisaiice oq
the Llandeilo flags and Caradoc sandstone are clearly the equivalent of these groups. — bs
It is here that we first find a number of species identical with European ones, and’
which enable us to institute a comparison. It will be found, however, that the ve
species in the Hudson River group correspond most nearly with the European forms, a
and that it may be doubtful if the base of the Trenton limestone has been reached in |
Great Britain.! . ; Fe

The Clinton group, with its beds of Pentamer us oblongus, represents what i in Eng- “2
land is regarded as the upper part of the Caradec sandstone; but we find it not. a
only above this well marked horizon, which we have ee indicated, but asso- —
ciated with numerous species of fossils, some of which are known as upper Silurian 2
forms in Europe, and others pass into forms characteristic of the Niagara group | ly x
this country. . 4

The Niagara group, with its shale and limestone, would seem, at first view, to be —
the exact equivalent of the shale and limestone of Wenlock and Dudley in England, —
and of Gothland in Sweden,so numerous are the identical species in these Eros 8
but on examination we find that there are numerous species included in these rocks |
in Europe which occur only iz the lower Helderberg limestones, and which are ~
separated from the Niagara by the enormous deposit of the Onondaga salt group. —
It is clear, therefore, that in the Wenlock formation of England and its representa-_
tives in northern Enrope are included parts at least of two distinet groups in 1 the |
order of time—distinct both in their physical and zoological features; and we can
not institute a proper comparison between the rocks of our own cptuntey and those ?
_of Europe while we regard that as one group. The condition, both in England and
on the continent, is doubtless similar to what we find in Tennessee and Virginia,
where, from the absence of the intermediate groups not only the Niagara and lower
Helderberg are united together, but even the upper Helderberg Limestone: are
superadded.,? 2

Barrande.—A ereolating based upon paleontologic data was eau by |
Mons. J. Barrande, in 1853, between the formations characterized by the
first, second, and third fauriad of Europe and those included in the
Silurian of America. In commenting upon the identification of ‘the
Russian Obolus apollinis Kichwald, by Owen, with the Potsdam sand
stone species of the Upper Mississippi Valley, he says: ~ —

In fact I am inclined to think that science has passed out of the epoch when it was”
thought necessary to have identical species in order to recognize equivalence of * geo- ie
logic horizons, even at great distances on the earth’s surface. The distribution of our 7

present fauna teaches us that this means can not be. altogether. relied o1 on to prove -
strata contemporaneous.

1 Op. cit., pp. 295, 296. 2 Op. cit., p. 299. 2
®Barrande, J: (Silur-fauna in Wisconsin und in New York.) Neues Jahrbuch fiir Miner. 1858, f le

(RRO RETESET, 079 51 LS, oh ell se ‘ ;
fon ase . Md! a ee T ts FX, , ‘ P Feat a ee. ~
Ping -.. yet ¥ - ¥ x ree « 5. x. -* 2
CEs Gaiety eK j hs : a :
as “bs nts es yy t ‘ Z : :

~

wacom] = = ~~ ~—s CORRELATION. cs
eae ‘ :

»

‘The fact that the Paleozoic formations of America during the appearance and dis-

appearance of three successive faunas, which despite some common species are on the

~~
*

whole well distinct, teaches us that the extinction and appearance of beings on the
earth’s surface are by no means determined exclusively by the physical revolutions

of the crust, but are ordered and regulated by the laws of animal creation itself.
Still, it is not my intention to follow out this consideration, as it would lead me too

far. I merely wished to mention this, in passing, as a subject for further study, and

oi to point out to investigators that paleontology leads to the establishment of a geo-

logic chronology, independently of the more or less local revolutions which the fossil-
iferous strata have undergone since their deposition.!

From a study of the faunas of the two countries he considered that
the first, second, and third faunas of Bohemia are to be identified in
America; that there exist manifold relations in all classes of animals of

the Upper Silurian division of the United States and Bohemia; that,

in the first volume of Hall’s Paleontology of New York, on the Lower

Silurian division, from the Potsdam sandstone to the Hudson River

group inclusive, he recognizes the First Silurian fauna of Bohemia,

_ Sweden, and England ; that the presence of the long-missed first fauna
of Bohemia in America has been demonstrated in a very satisfactory

-manner by Owen in his discoveries in the northwestern United States ;

and that the occurrence of this fauna in the State of Georgia is indi-
cated by a Conocephalus brought to England. In conclusion, he says:

Hence I am now perfectly convinced that the Silurian formations of North Amer-
ica, as well as those of the old continent, contain a succession of three different faunas, —
which, on being separately compared with the latter, are seen to consist of the same
geologic elements and to follow each other in the same order. When I say that they
consist of the same geologic elements you know already that Iam far from wishing
to maintain identity of species. I rely on other more general analogies which to me

are not less convincing. This is not the place to explain this more in detail, as that

would lead me too far; but you will find here and there in my work some passages
which express my view of the matter. In admitting and recognizing in all Silurian
regions of the two continents three general faunas corresponding and equivalent to

each other, I am induced by the facts to pronounce a further result of my investiga-.

“eh

tions, namely, that the local divisions of strata containing these great faunas, though
greatly differing from each other in each region of a certain extent, are not equal to
each other in the various countries, especially when the countries are far apart, geo-
graphically. This truth seems to me solidly established by a multitude of facts
which are tabulated and compared in my geologic sketch, and is confirmed in a very
‘satisfactory manner by the facts mentioned in volume 2 of J. Hall’s Paleontology of
New York.?

_ Rogers.—In a paper read before the British Association for the Ad-
vancement of Science in 1856, on the correlation of the North American

and British Paleozoic strata, Prof. Henry D. Rogers described the

Paleozoic section of the Appalachian region and that of, England, and

- instituted comparisons between them, to show the parallelism of the

North American and European Paleozoic rocks.2 He says:

In attempting this correlation it should be remembered that nature represents no

true or literal equivalency of strata, nor anything closer than a mere approximate

_ Op. cit., p. 339. 2Op. cit., p. 345.
_ $0n the correlation of the North Americar and British Paleozoic strata. British Assoc. Adv. Sci.,

; _ vol. 26,1857. Trans. Sec., p. 184.

;
~

Bull. 81 27

418 i ee _ THE CAMBRIAN. aa ie
relationship where the deposits compared belong to independent iin or even to |
the remote sides of the same great receptacle. The most we can hope to establishis _
a general agreement in time, with possibly a stricter synchronism of the few chief yi
paroxysmal movements which agitated the bed of the ancient ocean. Partially rep-
resentative formations are discoverable, but equivalent ones are not to be looked for
upon any philosophical view, since the distribution of organic beings is essentially .
partial or geographical. The life horizons of the globe are no more universal than |
are its horizons of sedimentation. With these reservations we turn to the degrees of -
affinity, linking the American’and European Paleozoic groups of fossils. Ry

As the result of his correlation he concludes:
nh
of Barrande’s Primordial zone and the lowest rocks of Russia and —
;

we

(a) The Appalachian Primal series is obviously nearly on the horizo
Scandinavia.

(b) The ‘Appalachian Auroral strata may possibly be approximately ia
contemporaneous with the Swedish Orthoceratite limestone. The _
Auroral series includes the Calciferous, Chazy, and Black River groups. — 4
(c) The Matinal series of the Trenton and Hudson River groups,
from the testimony of the fossils, are represented in Britain by the
Llandeilo flags and Caradoc sandstone, or more generally by Sedgwick’s —
Bala or Upper Cambrian group. He also finds anear equivalent in the
Orthoceratite limestone of Sweden and Russia and in the Graptolite
shales. The authority of Prof. Hall is cited to show the paleontologic |
similarity of the English and American formations.
(d) The Levant or Medina group does not apaar to be cope in
Europe. ‘aa
(e) The Surgent and Scalent series, or Clinton and Hiab are com-
pared with the British Wenlock strata.
(f) The Pre-meridian series or Lower Helderberg. He quotes Mr. —
Hall as saying that he agrees with Mr. Sharpe and regards the Lower — 7
Helderberg strata as representing the Wenlock formation of England,
while M. de Verneuil considers them as equivalent to the Ludlow. He
then proceeds to correlate the Devonian formations with those of Hu-
rope. ° er en
His final conclusion is: ee
From all the foregoing facts and statements we arrive at this general inference, —
that upon both paleontological and physical evidence there is no well marked Silu-
rian-Devonian break discernible in the North American basin, no proof of an epoch |
or general interruption in the life-stream, with wide crust disturbance in the middle
Paleozoic ages, such as that which in earlier times, in the morning of the soeapieonicn a
- day, at the Cambro-Silurian transition, revolutionized alike the entire extent of the

American and European areas, both in their inhabitants and in their physical geog- 7 4
raphy.!

q
}
a
J

Bigsby.—A most elaborate comparison and correlation between the
Paleozoic section of New York and that of Wales was made by Dr. J. _
J. Bigsby in 1859. He observes that “ both these geological areas ap-
pear to have been constructed on the same great comprehensive prin- —
ciples and nearly of the same material, two most important considera- aM

1 Op. cits, p. 186.

ie

inh aig, a
z 9

ui
;

: ‘ "S
hike
a.
ih
A

a4
a. .

* Fans
. '

_ .

.

42 js
Ss

ake
>

RR oy 2

watcorr.}_ ie ie ‘CORRELATION. | 419

have received different dynamic treatment, in the frequency of plutonic
disturbance in Wales and its comparative absence in New York, such
_ dynamic treatment involving, it must be kept in mind, both gr aduhl and
sudden changes of population. While the strata of these areas are
formed of much the same mineral substances, the conditions of bein
their order, and quantities are very varied.”.!

He sums up the points of zoological similarity under the following

Bt
$5! tiv tions. One very great distinction between them, however, is that they
¢

heads:

(1) The organic remains of both basins belong to the same orders and genera, un-
mixed with those of other sedimentary systems, as Permian, Jurassic, ete.

(2) Vertebrate animals were introduced at nearly the same date.

(3) The organic remains approximate closely in general facies.

(4) They affect strata of the same mineral character in both, the majority prefer-

_. ying the calcareous, the others the arenaceous form of deposit.

(5) The great majority exhibit the same order in their introduction and distribu-

ec tion. This is seen in Orthis, Pentamerus, Spirifer, and other Brachiopoda, and in
_ Endoceras, Graptolites, Trilobites, etc., the more highly organized being often prom-—

inent in the early stages.

(6) The law of divergency into several matrices is the same, or ashi, so, in the
two basins, the number of instances being fewer in New York.

(7) Lhe great majority of animals typical or recurrent in one basin are so in the
other.

(8) The great majority of the recurrent fossils in both occupy the same number of
epochs, many or few.

(9) The great majority observe the same process or - law of increment and decre-
ment. This takes place in nineteen out of twenty-four orders and genera.

(10) The two basins have 108 organic forms in common, including most of the gen- —

era.

(11) The same orders and genera are rich and poor in species.
. (12) There is the same limited admission of Silurian forms into the Devonian SYS-
tem in New York and in Europe.

(13) The plants of both are typical, with one or two exceptions, °

Such are some of the great points of similarity. Now as to dissimilarity. Those
which arise out of the mineral character are partly owing to physical disturbances
and to a certain amount of metamorphism undergone by the Welsh strata. The
paleontological differences are many, but small, often merely individual, and they
seldom affect principles. They are due to the varying sea depths and other well

‘ known conditions.
_ The facts just recorded certainly indicate a close connection in nature and mode
of formation between the basins of New York and Wales. They seem to be quasi-

equivalents—the same, but other, to use a short, but convenient phrase in common

_ use.”

A

Agassiz.—When commenting upon correlations made between the
Paradoxides zone of Newfoundland, Massachusetts, and Scandinavia,

_ Prof. Louis Agassiz said :

That there may be synchronism of deposit without identity of fossils must be evi-
dent if we glance at the present distribution of animals. If at the present epoch
the fauna of America and Australia should become fossilized there would not be the

slightest resemblance between the representative species of the two continents. The

! Quart. Jour. Geol. Soc., London, vol. 15, 1859, p. 292. 2Op. cit., pp. 292, 293.

-

ry Nk eg OE Cae RE Ne eye en AR A SENT ORR FF Pe a a iti aa Se. Oe ae

a af ra - ' 4 ate, _ bs My J ¢ ai : af at ig" v e. * ae 4 an ae

: / : +4 , ‘. ‘ =a Vie Ts 3 _ M > e: ie oe ‘Ai, gta iar

rae BG Y RCE ie, Mel tan ges Se ae

4 at , ae ee aS a eee oh ee ee eae

420. | THE CAMBRIAN. ee [BULLS

paleontologist must be ready to admit that very different fossil faun» may be con- vie:
temporaneous, and that their difference does not necessarily imply a distinct zoolog- _
ical age.! ;

When discussing the typical forms and the distribution of the rocks_
of the Cambrian, Mr. J. J. Bigsby presents a table showing the order
of succession of the Cambrian rocks in various countries.? In this he
includes the Upper Cambrian sandstones of Texas and Nebraska, and
they are referred to the upper or Primordial division of the Cambrian.

Matthew.—During the progress of his extended researches in the
faunas and rocks of the Cambrian system in New Brunswick, Mr. G.
F. Matthew has had frequent occasion: to compare the stratigraphic —
succession and the faunas of the Cambrian of New Brunswick wi
that of Europe.

In a paper read before the British Association for the Advancement |
of Science in 1884, he correlates the fauna of the St. John group of
New Brunswick with that of the Cambrian of Wales, and concludes:
that it shows closer relations with the Solva group than with the Me-
nevian.? in

Near the close of the same year he stated i in a paper read before the
Natural History Society of New Brunswick that the discovery of a
higher fauna enabled him to correlate the beds containing it with the
Menevian group of Wales.‘

In an essay on the classification of the Cambrian rocks in pee
Mr. Matthew considers that the Potsdam sandstone is equivalent to
the Ceratopyge limestone, or the Tremadoc group, and represents the
upper part of the Tremadoc, as the Georgian series probabiy does the |
lower. This correlation is made upon the interpretation of the charac-
ters of the genera of trilobites in the American and European rocks.

A second paper on the classification of the Cambrian rocks in Acadia
appeared in 1889, in which a comparison of sections in Sweden and
New Brunswick with the characteristic sections of Cambrian rocks in~
Europe and in North America is made.’ In the comparison of sections
of Sweden and New Brunswick the base of the Paradoxides beds is taken
as the datum point and it is shown that the pre-Paradoxides horizonis _
_ present both in Sweden and New Brunswick, and thatthe Upper Cam-
brian or Olenus horizon is represented in New Brunswick by Stage 2.
of the St. John County section and by the same stage in Sweden. In
the second table of the sections of the Cambrian rocks in Europeand in
North America, the correlations made between the sections of Sweden
and New Brunswick are accurate and valuable; but those between the

xs

_ -.

,

*

te “

On the difference between faunas of zoological and geological Bers Boston Soc. Nat. Hist., ; if
Proce., vol. 8, 1862, p.58. BS

2On the Cambrian and Huronian formations. Geol. Soc. Quart. Jour., London, vol. 19, 1863, p. 44. a

3The geological age of the Acadian fauna. Brit. Ass. Adv. Sci., Rep. 54th meeting, 1884, pp. 742, 743.

4An outline of recent discoveries in the St. John group. Nat. Hist. Soc, N. B., Bull, No. 4, 1865,
p. 101.

5 Canad. Rec. Sci., vol. 3, 1888, pp. 79, 80.

® Canad. Rec. Sci., vol. 3, 1889, pp. 308-311.

Sap

Mg

CORRELATION, | A421

Par epterri North American sections of the Wasatch, Nevada, Highland
base. and Eureka are more or less defective, owing to the Fd as
interpretation of the paleontologic data.

The next essay upon the correlation and comparison of the European

Y -. 3 FA

formations with those of America by Mr. Matthew is entitled: «‘ How is | |

the Cambrian divided?—A plea for the classification of Salter and

Se | Hicks.”?} He institutes com parisons of the strata in Wales, Newfound-

land, and Norway,and of the characteristic trilobitic genera of each
horizon. From the results obtained by these comparisons he considers
that the Cambrian is to be divided into the Upper and Lower, and that
the method proposed by Mr. C. D. Walcott, of separating the Olenellus

ey . - ~ ; 1
_ or Lower Cambrian from the Paradoxides or Upper Cambrian, is not

justified by the evidence afforded by the American and European sec-

. tions.
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ie i as . METHODS OF CORRELATION,

I. Superposition.

II. Organic Remains.
_ II. Lithologie Characters.
- IV. Unconformity.

V. Miscellaneous.

I. SUPERPOSITION.

(a) The order of superposition of strata is the foundation of geologic
chronology. By its aid the stratigraphic succession and serial relations

_ of the fossil faunas are first determined. Undisturbed superposition -
; within a section is an absolute test of relative age of the parts of that
‘section; it is not positive evidence of the age of the various beds in

_ relation to beds sustaining the same serial relations in some discon-
nected section without other tests to support it, even though they

occur in the same geologic province: e. g., a band of sandstone beneath
a limestone and above a shale may be identified in one portion of a
geologic province; but the occurrence of a band of sandstone beneath
a limestone and above a shale, in a distant portion of the same province,

__. is not positive evidence that the two bands of sandstone are synchro-
- nous or portions of one continuous formation, unless their continuity

can be traced.
(b) Superposition is not a test of identity of formation except in a

limited basin, where the geologist has evidence to show that the forma-
_ tion is practically continuous in its stratigraphic relations. In widely

4
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4

éy el portions of the same basin, or of different basins, the order

of Superposition must be sustained by other tests before it can be as-
_ Berted positively that the formations thus correlated are identical.
(c) In the same geographic or geologic province, fresh-water and

- marine deposits are not to be correlated with each other, even if they

1Am. Geologist, vol. 4, 1889, pp. 139-148.

:
F: Sake. She .

aoa ¢ THE CAMBRIAN. hs ae ee

have the same order of superposition, as the conditions under which ae “-

they were accumulated are entirely dissimilar, and the proof of the
contemporaneity of deposition is not available. An exception to this’
may occur where a stream passes through a lake and carries the fauna
and flora to the sea, where it is mingled with the marine fauna. !

II. ORGANIC REMAINS.

There are several considerations always to be borne in mind in corre-—

lating a formation on the evidence of. its contained organic remains:

(a) There can be no scientific or systematic paleontology without a

stratigraphical basis.!

(b) The method of correlation by the comparison of fossils; or, as it
has been called, “matching,” is the one that affords the best fesults.
It includes the comparison of species, genera, families, and the general
facies of a fauna. It is the basis of paleontologic correlation and geo-
_ logic elassification of the sedimentary rocks, with the exception of the
stratigraphic and lithologic correlation of local formations.

‘(c) In nearly every section of strata there are considerable thick-
nesses of beds, in which, no fossils are to be found. These beds occur
in nearly every formation. The record of life, during these nonfossil-
iferous periods of sedimentation, is broken.

_(d) Many fossils have a great vertical range; and the occurrence of
a few species of this character without the presence of species of known
limited range can not be taken for the identification of any particular
formation. If the laws of constancy and variation of the wide-ranging

and long-enduring species are known, it may be possible to use them in —

the correlation of minor formations, and thus create an exception to
the general rule.

(e) All paleontologic reasoning is based upon known data. By the
discovery of a new grouping of fossils, or a different range of known ©

species, the identification of horizons may be materially modified.
(f) In correlating a formation it is necessary to exercise caution be-

may vary in its constituent parts and afford different groupings of
species in localities not far distant.

(g) All correlations between widely separated provinces are based $ .
upon the general and not upon the specific character of the fauna; i.e.,
it is the general assemblage of a fauna in one basin that is compared ri 4

with that in another basin.

Within limited areas the comparison of species and the grouping

of species suffice to’ determine some particular horizon or formation.
In widely separated parts of the same area or province there will

1Hall, James. On the Primordial fauna and Point Levi fossils. Am. Jour. Sci., 2d ser., vol. 31,
1861, p. 224. ©

A
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fore deciding that the contained fossils belong to any specified zone of
the fauna characterizing a terrane or group of formations, and thus _
locating the exact stratigraphié horizon of the formation. A fauna

as

‘a
> .

BE eat teres _ CORRELATION, Ce Rae

a be a greater dittenaricn in the species, and the general or the spe-
a a “cific grouping of the genera will have to be taken as the data for com-

parison. In separate provinces the species may be the same in some
instances; but it is by the comparison of representative species and
- genera that the correlations are to be made. In provinces separated
is great distances, or upon two continents, the general assemblage of
the characters of the two faunas are to be compared. It may be
accepted as a general rule that the more detailed the comparisons are
the more restricted is the area in which specific results are of value.
The results, however, may be of the highest value in strengthening a

- correlation based upon representative types. The exception to this is

_ the occurrence of similar life zones in widely separated regions.

_(h) Zoologic provinces have been more or less limited in area from
the beginning of Paleozoic time. This is shown by the character and
distribution of the earlier Cambrian fauna. The provinces were as dis-
oy Maeity. marked then as at any time during the deposition of the Pale-
_ oz0ic.

(t) Many of the earlier zoologists and paleontologists prior to the

| _ period of Darwin studied the strata and the contained fauna with the
view that each group of species had a greater or less distribution and

were then suddenly exterminated, a newly created fauna taking its

place. This enabled them to correlate their formations with great
- accuracy, and to differentiate them upon the evidence offered by the

occurence of a very few species.
(j) The environment or condition under which the faunas lived and
were deposited is also to be noted. Whether they were littoral or

2 pelagic, whether they lived in cold or warm water, upon a sandy or a

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muddy bottom, in salt or in fresh water, are all considerations which
must be taken into account in discussing their value as factors in cor-
relation.

(k) The presence of recurrent faunas in strata lithologically similar

may give rise to imperfect and erroneous correlations. This is not
liable to occur except in a limited geologic basin, where the conditions

of sedimentation were uniform over large areas, and the environment

- of the fauna such that it continued, under favorable conditions, in some

- portions of the basin, and occupied other portions intermittently, as

the varying phases of sedimentation were fayorable or inimical to its
‘distribution.

(l) The relative age, serial relation, or homotaxis of sedimentary
- formations is best determined by the marine faunas, as the conditions.

fe under which they lived and were deposited were much more uniform
_ than those surrounding the terrestrial fauna and flora.

‘The evidence furnished by paleobotany is fragmentary, and its se-

- quence is so interrupted by nondeposition and nonpreservation that
- no comparisons of great value have been established by its aid. What

_is true of paleobotany is also true, to a less extent, of terrestrial faunas.

sneha at) Raitt tate Paha aaah SBR Cr MS ete NC Mie gu al M9 “We PI Nee
Shi 4 a a ‘THE CAMBRIAN. — * mie, he “trou mon

4 x“

It is ate by dedabuit and through peculiarly favonable jonalaha that’ om
land faunas have been preserved. With the marine faunas on the con- "4
trary the opportunities for the preservation of the fauna of each epoch —
were far greater, and the conditions of environment were more favorable _
for the uniform advancement and evolution of life over extended areas.
Life-zones.—The proof of the presence of life-zones in the geologic

Series is one of great importance in correlation. The subject has been
so ably presented by Prof. H. A. Nicholson that I will quote it in full ~~
in preference to giving a synopsis of it or to presenting my own views, a
which accord essentially with those of the author. He says:

While each geological rock-system is characterized by a general assemblage of dis-
- tinctive types of animals and plants, the minor subdivisions of each system are like-
wise distinguished by the prevalence of particular forms of life. There are no doubt
cases in which an extensive series of successive strata may appear to be characterized
throughout by essentially the same organic types, there being apparently no restric-
tion of special fossils to special horizons in the series. In so far as such cases have
any real existence, they may be explained as instances in which a great series of sedi-
ments has been accumulated with such rapidity that there has been no time for e
marked biological changes, resulting in the dying out of old species and the intro- 4
duction of new forms. In many cases, however, the apparent diffusion of the same —
kinds of fossils from the base to the summit of a series of beds perhaps two or three
thousand feet in thickness is due simply to the fact that the organic remains met
with in the formation have not been sufficiently investigated and that the exact
horizon at which each occurs in the series has not been accurately determined. The
determination of the horizons of particular life-forms is a work of time and demands
both great stratigraphical knowledge and also a wide and accurate acquaintance
with the characters of the fossils themselves, two requirements rarely fulfilled in the
same individual.
In a considerable number of cases, however, it has now been shown that the fossils

of a given formation may be divided into two principal groups. In the one group is
comprised a series of common forms of life, which may be regarded as characterizing
the formation as a whole. In the other group are included certain special fossils con-
fined to particular parts of the formation and characteristic of certain definite hori-
zons or zones, Within the limits of theformation. All the great formations are to some
extent capable of being broken up into minor rock-groups, characterized by special —
life-forms. Some of the differences in the kinds of fossils found in different parts of
the same formation must, of course, be simply set down to the fact that different
kinds of sediment imply changed conditions in the sea, and hence changes in the
marine fauna. If, for example, part of a formation consisted of limestone and part of
sandstone, we should expect, beforehand, to find that each of these rock-groups would
have some fossils not found in the other, since the two would have been formed under
different conditions. Apart, however, from differences arising from causes of this
nature, we meet with cases in which a formation, even if essentially homogeneousin
its mineral nature, can be divided into zones, sac of which is characterized by the
possession of special groups of fossils. Organisms belonging to any class of animals
may serve in this way as test forms (‘‘ Leit-Fossilien ”) for special horizons in a series
of stratified formations, but there are paiticular groups of fossils which have been
_ found to be preeminently available for this purpose. Among the older rocks of the
earth’s crust, the forms which have proved specially valuable for the determination
of particular “zones” are the Graptolites, the Trilobites, and the Brachiopods, while :
the Cephalopods have been found to afford the most satisfactory tests in the case of | yi
the Secondary rocks. A well known instance of this subdivision of a system of strata
by means of special types of fossils is that afforded by the Ordovician and Silurian

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rocks of Europe, in which a OATSE Ata following Professor Lapworth, have recog-

_ nized numerous well marked ‘life-zones,” characterized for the most part by the
possession of particular types of Graptolites, though, in some cases, the distinctive
- fossils belong to other groups Another well known eek ple of the same phenome-
non is afforded by the Jurassic deposits. These have been shown to contain a num-
ber of well marked zones, each of which is characterized by the possession of some

: ‘special fossils, and particularly by some special Ammonite. These zones are extremely

constant in any particular region, and they enabie the observer to effect a division of

the formation into special horizons, which have no stratigraphical existence and are

not separated by any physical break, but are of the utmost paleontological impor-

_ tance and can be rendered readily available in working out the stratigraphy of any
_ given area.

Certain life-zones appear to have nothing more than a local development and im-
portance. but in other cases they have proved to be astunishingly constant even over
very large areas. Perhaps the most remarkable known instance of the extension of

- particular life-forms over a vast area is that afforded by the Arenig rocks (a subdivi-
gion of the Ordovician system), which have been recognized as occurring in Eurupe,
in Canada, and in Australia, and contain in all these widely remote areas the same
_ peculiar types of Graptolites.

The principa! difficuity that we have to confront in dealing with these ‘‘ zones” is
to produce any plausible explanation accounting for the destruction of the special

life-forms of the one zone and the appearance of those of the next zone. For the most
_ part, these zones are of very limited vertical extent, and they succeed each other in

such a manner as totally to preclude the idea that the dying out of the old forms can

have been in any way caused by a physical disturbance of the area. Perhaps the

most probable view to adopt in the meanwhile is that the formations in which dis-

tinet and limited life-zones can be recognized were deposited with extreme slowness,

whereas those which show an essentially compact and homogeneous fauna from base

to summit were deposited with comparative rapidity. Upon this view, a formation

like the Lias is one formed by a process of very slow and intermittent sedimentation,

‘the life-zones being separated by intervals during which sedimentation must have

been at a standstill, but which were long enough to allow more or less considerable

ce biological changes, some forms dying out or becoming modified while other new ones
came in. Upon this view, further, a formation like the Lias, though of compara-

tively small vertical extent, may represent as long a period of time as the whole of

_ such a great formation as the Lower Carboniferous, which appears to have been

me,
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_ formed under conditions of comparatively rapid sedimentation.'
Life-zones have been determined in the Middle Cambrian or Para-

doxides terrane of Sweden, Wales, New Brunswick, and Newfoundland

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or the Atlantic Basin Province. In a broader range the genera Ole-
.nellus, Paradoxides, and Dikelocephalus are considered typical of the

_ three primary zones or divisions of the Cambrian group. They are of
unequal value and decrease in precision from the older to the later
faunas. The genus Olenellus has a’ wide distribution in western Eu-
- rope and North America, while Paradoxides is more limited in Amer-
ica, and the true Dikelocephalus probably has a still smaller geo-

| pepuuiniic range.

Stage of evolution.—The evolution of organic life is a factor in corre-
Pave that has been assuming some importance within the last few

years. To be of practical use the paleontologist must have a thorough,

) General Introduction, Manual of Paleontology, by H. A. Nicholson and R. Lydekker, vol. 1, 1889,

pp. 58-60.

CORRELATION. 425

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accurate knowledge of the species and divair life histone: inetusdine a
of the genus and family to which they belong. Types of restricted

range and short-duration are of little importance, except as expressing —
the stage of development of their genus. The persistent, long-enduriug ©

types, that range from formation to formation and even from group to
. group, may be of service if their study and analysis have revealed
characters by which their relative stratigraphic position, in a given
area, may be determined. The evolution of genera is of greater value,
and the analyses of the development of specific types within them may
be used in the identification of horizons. é'

Extended to groups of genera, families, or orders, correlation by the !

known evolution of the faunas may be used in a general way. In the
presence of other reliable data it is of relatively small value. Only in

instances where there are no other data that can be made available will

‘it be really of practical service to the geologist.

Even under the best conditions and circumstances creat care must oe
be used, owing to the varying conditions caused by environment and ‘i |
the Naat evolution of organisms in different geographic areas or |

- basins. I do not wish to imply that this method of. correlation should
be entirely overlooked or dismissed in the presence of more reliable
data. It can be used in connection with other methods in correlating
any formation or group of formations, but only in extreme cases should

it be considered the only factor. When used, the result Bebe sy can

be considered as little more than provisional.

Life history.—A careful study of the life history of the various ele-

_ ments of the faunas promises to yield data that may be important in
correlation. An illustration of this is afforded by Prof. H.S. Williams’s

study of Spirifera levis.'' This is a type that is represented by various |
forms from the Niagara limestone of the Silurian to the summit of the
Devonian, that are evidently descended one from the other, although
they have been described under several specific names. Ateach ho- —
rizon the variation from the initial form serves to locate its stratigraphic — .

horizon and thus its relative age and position in space and time. The

tracing of the migration of forms from one area to another and the
changes produced upon them during this migration are to be taken
into consideration. The theory of Prof. Alpheus Hyatt,’ that there is
a cycle of forms in the geologic series and a corresponding cycle of varia- —
tion in the species of that series and in the individuals of any one spe-
cies, may lead to practical results. He finds it to prevail very exten-—
sively in the Cephalopoda, and it will undoubtedly be found to apply —
_ to all the other zoologic groups. The conclusions obtained will be more _
or less marred by the imperfections of the geologic and life record, but —

I look forward to the time in the future when minute biologie studies

1 The Life History of Spirifer lwvis, Hall. Ann. N.Y. Acad. Sciences, vol. 2, 1881, pp. 140-160, pl. xiv.

2Genera of Fossil Cephalopods. Proc. Boston Soc. Nat. Hist., vol. 22, 1883, pp. 253-265. eh i many —

other papers by Professor Hyatt, referring to and describing the Cephalopoda.

Lee | ie: ae en

426 Lele! ey . . “THE. CAMBRIAN. Pape ee Cee ot micntee ona 4

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- G@ORRELATION. 427

ee of the faunas, in connection with a careful study of the sedimentation
and stratigraphy, will make our present methods appear to have been
4 > Waekking 3 in scientific precision.
- Contemporaneity and Homotaxis.—When it was once established that
a certain order of succession of fossils occurred in Europe, it was con- |
eluded that identical or similar assemblages of organisms would be
& _ found to prevail els¢where over the earth; and that the geographic
distribution of each successive fauna was wari wide, each fauna being -
anew creation. The present view is, that the chronologic succession
of the fauna is local, as proved by the existence of zoologic provinces,
and that each fauna is descendant from some preexisting fauna. This
a result is modified for each province by the migration of faunas and
= ara of faunas from province to province. Notwithstanding the
various elements that influenced the evolution of the faunas, itis found
| that the general succession of species and faunas is in the aggregate the
ts same all over the world, however much it may have been broken, ad-
_vanced,-or retarded in certain areas in ancient or relatively recent
geologic time.
Prof. Huxley, when introducing the term “ Homotaxis,” said:

tents of distant formations was prima facie evidence, not of their similarity, but of
’ their difference of age; and holding as he did the doctrine of single specific centers,
# the conclusion was as legitimate as any other; for the two districts must have been
ate" occupied by migration from one of the two, or from ,an intermediate spot, and the
x chances against exact coincidence of migration and of imbedding are infinite.
4 In point of fact, however, whether the hypothesis of single or of multiple specific

¥

=
4 _ Edward Forbes was in the habit of asserting that the similarity of the organic con-
3

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centers be adopted, similarity of organic contents can not possibly afford any proof
_ of the synchrony of the deposits which contain them; on the contrary, it is demon-
, _ strably compatible with the lapse of the most aodikiate intervals of time, and with
interposition of vast changes in the organic and inorganic worlds, between the epochs
in which such deposits were formed.! * * *
There seems, then, no escape from the admission that neither physical geology nor
off paleontology possesses any method by which the absolute synchronism of two strata
hry. can be demonstrated. All that geology can prove is local order of succession. It is
2 e mathematically certain that, in any given vertical linear section of an undisturbed
a 5 series of sedimentary deposits, the bed which lies lowest is the oldest. In any other
he ; -. vertical linear section of the same series, of course, corresponding beds will occur in a
ss - asimilarorder; but however great may be the probability, no man can say with abso-
be lute certainty that the beds in the two sections were synchronously deposited. For
ve areas of moderate extent, it is doubtless true that no practical evil is likely to result
# from assuming the corresponding bedsto be synchronous or strictly contemporaneous ;
Stee ‘and there are multitudes of accessory circumstances which may fully justify the
% om assumption of such synchrony. But the moment the geologist has to deal with large
mee areas or with completely separated deposits, then the mischief of confounding that
_ “Homotaxis” or “similarity of arrangement,” which can be demonstrated, with
pe ' “synchrony ” or “ identity of date,” for which there is not a shadow of proof, under
+ the one common term of ‘‘ contemporaneity ” becomes incalculable, and proves the
constant source of gratuitous speculations. %

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1 Quart. Jour. Geol. Soc., London, vol. 18, 1862, p. xlv.
2 Op. cit., p. xlvi.

428 THE ee

Tn this connection the student should read Mr. J. B. Mares’s paper on ie :
Homotaxis! | DP Ale

- Percentage of species.—This method of paleontologic correlation was — ,
employed by Sir Charles Lyell. He found a certain percentage of | *
species identical with living forms in one horizon, the Eocene; a larger ~
percentage in the Miocene, and a still larger one in the Pliocene. He
then concluded the Eocene represented the oldest and the Pliocene the
latest deposit. He thus classified the formations and gave an indirect
method for their correlation in different ‘areas. It is not capable of
application where all the members of a fauna are extinct. 5

Ill. LITHOLOGIC CHARACTER.

Lithologic character has very little value in establishing correlations, ©
when comparing formations outside of limited areas. The constituents —_
of a rock may differ in their chemical and mechanical condition in a
stratum that is proved by other evidences to be continuous. In some
instances lithologie characters may be of value, especially in areas
where the stratigraphic sequence of the beds is known and paleonto-
logie evidence is lacking. Dr. R. D. Irving used the method success-
fully among the pre-Cambrian rocks of the Lake Superior region, and
says of it:

-

Its value in tracing formations from point to point can hardly be overestimated,
being as great as that of paleontological evidence and, in my judgment, of much the ©
same nature. As we trace formations and their minor subdivisions from placeto
place we must of course constantly check lithological evidence by stratigraphy. As _
we pass from one extremity of the field to the other, changes in lithological charac-
ters of course come in, and these changes might lead to unsafe conclusions were we to _
compare stratal successions too distantly removed from one another; but when we :
work from point to point such changes are detected as they gradually appear, and
are provided for.? re

An illustration of the value of the method is shown by sii correla-
tions made by the brothers Roger’s’ in Virginia and Pennsylvania, where
they correlated the quartzites, shales, and limestones by their litho- _
logic characters along an extent of several hundred miles. When,

however, they came to carry this correlation without that area of sedi- — ,
meutation, the inadequacy of the method is shown by the fact they
correlated the Lower Cambrian quartzite with the Upper Cambrian

quartzite about the Adirondacks of New York. A still more striking ~
illustration of erroneous correlation by this method is that made by ~
Prof. N. H. Winchell‘ in correlating, as members of one formation, the a

Sots et Ae see SRE 2 te Sol So ge oe eR Se, 8 ee es a
1 Proc. Cambridge Phil. Soc., vol. 6, 1887, pp. 74-82. - a
? Seventh Ann. Rep. U.S. Geol. Survey, 1885-’86, 1888, pp. 378, 379. G
3 A system of classification and nomenclature of the Paleozoic rocks of the United States, with an
account of their distribution, more particular:y in the Appalachian mountain chain. Am. Jour. Sci, _
vol. 47, 1844, p. 112. a
4The crystalline rocks of Minnesota. General report of progress made in the study of their field.
relations. Statement of problems yet to be solved. Geol. and Nat. Hist. Survey of Minn., 17th ADR
Rep. for 1888, 1889, p. 49. a

eRe: Cambrian quartzite of the western slopes of the Green Moun-
os tains, the Upper Cambrian Potsdam sandstone of New York, the pre.
g Cambrian Sioux quartzites of Minnesota, the pre-Cambrian Baraboo

cali of Wisconsin, and the pre-Cambrian quartzite of the Kewee-
_nawan series of Lake Saperior.

: if Lithologic character is often of great value within limited areas and .

“eh where the formation can be practically traced from place to place. As
this can rarely be done, it is best to seek other data and to combine
with the lithologic, the stratigrapiic and paleontologic evidence, if itis
possible to obtain any.

IV. UNCONFORMITY.

Of all the data of correlation that of unconformity of the formation

CORRELATION. 429

2 _ correlated, with its superjacent or subjacent formation, would appear at °

Fig first sight to be the most unreliable. In most instances it is, but where

_ combined with other data it has acertain value. We find it used in the
Bots aha correlations made of the Potsdam sandstone of New York, with
ia the basal sandstone all along the Appalachian Range south through
: i New Jersey, Pennsylvania, Maryland, Virginia, Tennessee, Georgia, and

Alabama. It is also used in the correlations made between the Pots-
a dam sandstone of New York and the sandstone of the south shore of
Lake Superior, and the fossiliferous sandstones of Wisconsin, Lowa,

and Minnesota, that were correlated with the Potsdam sandstone by
Messrs. Owen, Hall, and later observers. In fact, it is implied in
; nearly all the references of strata to the Potsdam horizon in other local-
rer ties than that of the typical area about the Adirondack Mountains of

4 New York. It was not, however, until the appearance of Prof. R. D. Irv-
ing’s essay on the Maasilivation of the earlier Cambrian and pre-Cam-

og
brian formations! that full significance was given to the value of un-
- ¢onformities in correlation.

a _ The problem is presented by Dr. Irving as follows:

¢ (1) To determine upon the grander divisions (groups) to be ma de in classifying the
rocks independently of their relations to the general geological column; (2) to ex-
____ tend these divisions to other portions of the same geological basins; and (3) to cor-
we relate these divisions with those of different and distant geological regions. This is
fe the problem which presents itself in the Lake Superior region, at the base of the
Grand Cafion of the Colorado, in central Texas, Newfoundland, and in other por-
pra tions of North America.
ae In any attempt to solye such a problem we can make use of one or more of three
_ kinds of characteristics in the formations involved, viz: (1) their paleontological
a _ characteristics, (2) their lithological characteristics, and (3) their mutual structural

a ‘, - Telations.?
ei : Under the third title, “their mutual structural relations,” he con-

__ siders unconformity as a basis for classification * discussing the general
- nature and significance of conformities and the distinguishing char-

me
i 7
s

Fey: acters of true unconformities. A description is given of the Potsdam-

~) i
Ree a ap! 1 Seventh Ann. Rep. U.S. Geol. Surv., 1885-86, 1888.
rss? 20p. cit., p. 371. 30p. cit., p. 390.

such as to indicate periods of time only comparable to the periods necessary for

430 ik) oy) THE CAMBRIAN, 5- pieohs (DULL.

Huronian unconformity on the north shore of Lake Huron, the Pots- —
dam-Keweenaw unconformity, the Laurentian-Huronian unconformity

and others of the Lake Superior region. This is followed by a section

on the use of unconformities in classification. In this the use of un-
conformities in defining the grander groups of strata and in correlating |
the formations of a single geologic basin are discussed. Under the -
first, he says:

Returning to our problem as originally stated, we have next to Ml how far Ee

unconformaties may be made use of in defining the grander groups of stratain a
region in which the succession of these strata has been determined. Further argu-
ment than that already given in discussing the nature and kinds of unconformity is —
hardly necessary to show that genuine unconformities, indicative of great lapses of |
time between the periods in which the strata on either side of the break in each
case were respectively made, are of prime value and importance in determining the
limits of the grander groups of the geological formations, whatever use we may
make of paleontological and lithological characters in determining subordinate

divisions. Such structures as the greater ones of the true unconformities, above con- |

sidered, indicate lapses of time great enough to cover extended periods of mountain- .
making, always a slow process, and also great periods of denudation or exposure to
the atmospheric agencies. It is hardly possible for us to compare such time gaps
with the time necessary for the formation of definite thicknesses of strata, but the
thicknesses of strata corresponding to such breaks must surely always be very great.

If we take for instance the gap indicated by the relations of the Potsdam sand-
stone to the ancient gneissic formation of the northwest, as above illustrated by a
number of examples, we find that it was long enough to cover not merely one period

of rock alteration, orographic movement, and land surface exposure, but three such __

periods, between which were times long enough for the accumulation of thicknesses of

strata aggregating over 60,000 feet, a thickness exceeding that of the entire Paleozoic 4

series in its greatest development in the Appalachian region. It is true that a portion
of this 60,000 feet is made up of volcanic materials, chiefly lava flows. The accumu-
lation of such materials may, it is true, have been more rapid than is the case with
ordinary fragmental deposits ; but the accumulation of such a mass of eruptive
material must have occupied at least a considerable lapse of time; while more than >
one-half of the 60,000 feet, or an amount approximating the maximum Paleozoic ac-

cumulations in the Appalachian region, is made up of genuine detrital deposits. When |

we consider that in addition to the time necessary for the accumulation of this mass’
of sediment there intervened between the Potsdam and the gneisses three periods of
rock alteration, mountain-making, and complete mountain removal, it becomes plain
that the time gap indicated by this unconformity must have exceeded the entire Paleo-

zoic era. More probably, indeed, it equalled all later geological time. Each one of © ‘.

the three unconformities mentioned must of course have required a shorter period
than this greater gap, but in each case the relations of the several formations are

the accumulation of one of the great geological groups.?

The use of unconformities in correlating the formations of a single

geologic basin, where the exposures of the formations are not continu- ~ E
ous, is illustrated by a tabulation showing the general succession of —

formations in various districts from the northern end of Lake Huron to —
Dakota and from central Wisconsin to the north shore of Lake Superior. —
This table shows that in various localities there is a great unconformity

1Op. cit., p. 438, ? Op. cit., pp. 438, 439,

ae . - -- CORRELATION. 431

between the Laurentian and the Huronian, between the Huronian and
~ the Keweenawan, where the two series of rocks are present, and be-

tween the Keweenawan and the Cambrian if these two occur in the same

oy area.

____ _ He next takes up the use of unconformities in establishing general

" - relations. Under this heading we quote as follows:

m4 Having established the general order of succession and the grander groups of the
strata for a given geological province, the question which arises next in order is how

¥ to correlate these divisions with those of other geological provinces, and more partic-
warly with the established divisions of the general geological column.
eA It will take but little consideration of the causes which have been at work in the

pone) production of such unconformities as have been above cited to make us realize that
~__ such breaks as these must be widespread in their influence. Great unconformities,
in which the strata below the unconformity have been subjected to folding, mark
-__ periods of orographic movements which will, in general, have been extensive some-
what in proportion to the intensity of the folding process.'
are It is well known, indeed, that some of the greater physical breaks in the strata of
-_ one continent may have their parallels among the strata of another continent. The
___ interruption between the Paleozoic and the Mesozoic is intercontinental, if not world —
_-wide. Equally extensive is the great break between the Mesozoic and the Cenozoic.
7 Each of these physical breaks corresponds to an immense change in life conditions.
_ But, if we may judge from structural relations, from the amount of intervening
s denudation, and from the rank already attained by the life of the lowest of the fossil-
sf iferous Cambrian formations, neither of these great breaks corresponds in length of.
_ time interval to the break between the lowest of the distinctly fossiliferous forma-
tions and the youngest of those beneath it.?
¢ _ The great structural breaks furnish, at times at least, a more trustworthy guide.
) If, for instance, we make a comparison of the succession of Cambrian and pre-
s % Cambrian strata in the Lake Superior region with the succession revealed in the
eat - depths of the Grand Cafion of the Colorado, we find some singular correspondences
___ between the structural breaks of the two successions. In each one of these regions
¥ 3 the Potsdam sandstone is strongly characterized by its well known fauna. In each
region the sandstone traverses the edges of a gently bowed but deeply denuded
formation composed of a great thickness of detrital and eruptive materials. Below
* these formations in each region, and separated from them in each case by one of the
strongest of unconformities, is a great quartzitic series, while below this series
again in the Lake Superior region, and separated from it by still another of the most
. notable of uneonformities, is the great Laurentian gneissic series. That this series
x also exists in the base of the Grand Cafion we have good reason to believe,
‘ “Such a striking similarity in succession as this certainly most strongly suggests the
SGP: conclusions that the physical breaks of the two regions were coincident in point of
time (that is, that the mountain-making movement which preceded the deposition
of the Potsdam sandstone of the Lake Superior country corresponded with that which
preceded the Tonto sandstone of the Grand Cafion region); that the mountain-mak-
. Be pi _ ing periods preceding the deposition of the Grand Cation series of the Grand Canon
. ae ‘district and of the Keweenaw series of the Lake Superior region were equally syn.
chronous; and, finally, that the Grand Cafion series is, in general, the equivalent of
ie s - the Keweenaw series, while the pre-Grand Cation rocks are the equivalent of the
Lake Superior Huronian.
~ Of course such correlations as these should be made, for the present at least, some-
__ what provisionally; but, on the other hand, they must be taken as of much greater
3 value than correlations between distant formations established on feeble fossil
“evidence. 3

! Op. cit., p. 443, ? Op. cit., p. 444, 3 Op. cit., p. 445.

MY a RS Oe Oe oe me Ga ees nT te aa Be reel eves
PM ES ei nts SMALE a Gi do Shi Sy

se: pe: ’

432° >> Cy THE CAMBRIAN.

The question is asked, is the term Cambrian to stop at the first — a)

unconformity below the Potsdam sandstone? Is it to extend to the

second of those uncomformities, or to the third? Or is it to neha
finally, the lowest of the formations of the region?
He makes the following reply to these questions:

~at
All these usages of the term have been made. In taxonomical value the term Cam-
brian is designed, of course, to correspond to the térms Upper Silurian, Lower Silurian,

Devonian, Carboniferous, etc., which terms are based primarily upon the general con-

tinuity for each one of the pelea to which they correspond of similar life conditions.
In no case, however, has one of these terms been allowed to span any such unconform-
able break as the least of those beneath the Potsdam sandstone of the Lake Superior

region. Minor breaks in the succession have been included within a single one of
-

these geological groups because—although in every case of a physical break, even the
smallest, a corresponding break in life-succession is found—there have been found on

“3
at

¥

ine

.%

+

both sides of the break fully developed faunas of general similarity in characters; —

‘but no great break in the succession such as those with which we are now concerned

has ever yet been found to be spanned by a continuity of forms. The conclusion,

therefore, seems inevitable that we should not extend the term Cambrian over any
such break, at least until there shall have been found closely corresponding faunas

~
-

“

on opposite sides of the interval. Were such faunas to be discovered the greatness _

of the unrecorded interval would still remain, and we should have indicated only a
singularly long continuance of similar life-conditions. Even then the question might
arise as to whether continuity of life-conditions should outweigh the great lapse of
time indicated by the physical hiatus.!

7

Finally Dr. Irving states that

The structural breaks called unconformities are properly used in classification—

(1) To mark the boundaries of the rock groups of a given region.

(2) To aid in establishing correlations between the formations of different parts of a sin- ;

gle geological basin.

(3) To aid in the establishment of correlations between the groups of regions distantly
removed from one another; but caution is needed in attempting such correlations in
proportion as the distances between the regions compared grow greater.

They are improperly ignored:

(1) When the evidence they offer as to separateness is allowed to be overborne by anything |

but the most complete and weighty of paleontological evidence.?

-

V. MISCELLANEOUS.

'

~G

Homogeny.—A method of correlation that has frequently been used —

has recently been named by Mr.W J McGee “ Homogeny” or correla- .

tion by community of genesis.2 Mr. McGee defines it as follows:

The method of correlation devised to systematize the structure of the Coastal Plain’

combines the desirable features of the older methods, and adds thereto the interpre-
tation of the products of the several physical processes operating upon the earth’s
exterior.*

a
-
tC
on
’

hax.

The older methods mentioned are those of stratigraphic continuity, |

lithologic correlation or correlation by petrography, and paleontologic

1 Op. cit., p. 446. 3Am. Jour, Sci., 3d ser., vol. 40, 1890, pp. 36-41.

2Op. cit., p. 448. 4Op. cit., p. 36. | a

sae CORRELATION. 433
~ correlation. He considers that “the method involves a yet broader
~ eonspectus of phenomena and principles than the paleontologic method;

for in its application it is necessary mentally to restore the various

_ physical and biotic conditions of the past, just as paleontology vivifies

bs the fossils of past ages.” Again:+

fe” Tn discriminating the general and local genetic conditions it is necessary to ascer-
tain the relations between each formation and its newer and older neighbors, and to
interpret the record of each unconformity in terms of continent growth. By this
means the different parts of a formation may be found to represent not only general
community of genesis but community of beginning and ending; in short, entire com-
munity of structural relation. Each part of the formation then records in similar
terms the same episode in continent building and world growth.

Ms So, when a coastal plain formation is found +o represent general community of

* genesis and structural relation in its various parts it is considered homogenic, and
accepted as a record of an episode in geologic history. ‘The parts may or may not be
homotaxial ; one part may be slightly older than another part; but in a general way
it is contemporaneous throughout. Homogeny implies not only equivalence but
synchrony.

The principles of homogenic correlation have long been used in the
correlations of formations by geologists. An illustration of this is the
correlations that have been made of the Potsdam sandstones of New
York with those of the Mississippi Valley, the eastern slope of the
Rocky Mountains, the islands of Texas and Missouri, and the valley of

the St. Lawrence. In these correlations to subjacent and superjacent

_ formations, stratigraphic continuity, lithologic or petrographic resem-
blance, and similarity of organic remains have all been used.

Under the definition of homogeny, that is, correlation by community of
genesis, decided errors must necessarily occur unless checked by paleon-
tologic data. An illustration of this is the correlation of the Potsdam

| _ sandstone of the Adirondack Mountains of New York with the *‘ Granu-
Jar Quartz” of western New England and southeastern Pennsylvania,
and the Chilhowee sandstone of Tennessee. These sandstones are litho-

- logically alike, they were accumulated along a coast line, their petro-
graphic characters are the same, and the action of the waves upon and

_ the distribution by tidal currents of the sediments originating. from
similar crystalline rocks all point to a community of origin; in fact,
they did originate in the same manner. They have been correlated

i upon the characters mentioned for upwards of 40 years, but the study

of the fossil remains shows they are not equivalent or synchronous.

_ One represents the basal beds of the Cambrian system and the other

zi the Potsdam sandstone or the closing deposits of Cambrian time in the

om same area. I think that after we have fully proven to our satisfaction
the similarity of origin or the community of genesis we must still rely

a ‘upon paleontologic data for the final determination of geologic equiva-

Jence. For the determination of synchrony, except in a limited area,

_ there is little hope for satisfactory conclusions by any method yet de-

vised.

4Op. eit., pp. 38, 39.

i) Ball'31—28

ae spoaraphi, features 4 in correlations ght |
i “cate relative geologic age in the discussion “of

in dealing with the Lower Paleozoic it has thus -
‘ _ impossible to obtain the evidence of newer or older topogray tb
ee that are of value. Mr. G. K. Gilbert has used it successfu ly in.
ing the age of the Equus fauna of Lakes Mono and Lahonton «
fornia and Nevada.'

ie

a

.
o RES

\

‘ eS: : Sted 1U.S. Geol. Survey, Monograph, vol. 1, 1890, pp. <r

-) & ‘lhe ¢ \
trish f~. ' - }

Sag ate

ede ty GATE, eae ay ay
%
INDEX.
; A. Page.
. Page, | Attleborough, Massachusetts, E. Hitch-
De Acadian series, J. W. Dawson on........ 62 cock on limestone in. .- ot siete ro 73
; RE 8 epcnnc--caceee 248 T.S. Hunt on rocks at ...........-.-.- 73
; eee 303 | Auroral limestone, T.S. Hunt ON.----0-+- 127-128
formations correlated with..---...... 360 | Au Sable Chasm, New York, section. ...- 343-344
Acadian eran Aisbawn ........----.- 305-306 | Australia, Cambrian rocks of ..-.....---- 378-379
Adams, C. B., on quartz rock of Vermont. 95 | Avalon and Fortune Bay, Newfoundland,
rh MEIMUTTOMOMIIEOGK (o.0 5005-0 cccepce- ss 97, 250-251 section. ....-.--.------------+--+- 257-258
aa On Taconic slate...................-. 99
he fossils of red sandrock ....-..-.----- 150 B.
_ Adirondack subprovince, paleontology of 229-232 | Bailey, L. W., on rocks of New Bruns-
4 Cambrian rocks of ...........--.....- 341-347 WAG... diehdandt ota oodeenee aee 61, 64
Sener aeinINMEN OF ¢-.........-.-.-..------ 347 | Bakewell, R., on use of fossils in correla-
______ problems for investigation in ......-. 381 DPR ini :- nan: ie onda ecwesdeneeenene 397-398
Agassiz, A., on Lake Superior sandstone. 195 | Balcony Falls, Virginia, rocks of.......-. 136
Agassiz, L., on rocks of Braintree, Massa- BOCUUE Wis oa iawae yas aaa 293-294, 297, 298
ie Soh) &. SET kwaes ae 74 | Bannock Range, Idaho, section..........- 322
, on correlation by fossils...........-.-- 419-420 | Bar Harbor, Maine, rocks at...........--. 68
- Amiand Sowter, fossils from Quebec. ... 232 | Barrande, J., on fossils from Braintree,
[> Alabama, M. Toumey, on rocks of.....-. 146 Massachusetts.....-...---.ecece- 75, 88
4A E. A. Smith, on rocks of............-- 146-148 on fossils from Georgia slate......... 99
a Cambrian rocks of ....-.....- 146-148, 305-308 primordial fauna of Texas .........-. 234
Antelope Spring, Utah, section........... 320 definition of primordial.............. 243
3 4s compared with other sections........ 320 use of fossils in correlation........... 416-417
Anse au Loup, |’, Newfoundland, section .253-254 | Bayfield, H. W., on rocks of Straits of
yo | Appalachian province, definition of...... 91-274 Belie Tale: 2. 2. ..savst aide haces 5 50
a 2 Cambrian rocks of........-.--. 91-148, 274-312 on Lake Superior sandstone.......... 188, 252
. Archwocyathus, remarks on............. 319 | Beecher & Hall, on Mohawk Valley...... 207
Argentine Republic, Cambrian rocks of. SFR. t. Bellé Tala: Saleen seen bas ak ed eS 50, 51
- Arizona, Cambrian rocks of...... 219-221, 356, 357 | Belle Isle Straits, rocks of.........-----. 102, 104
ti J.S. Newberry on rocks of..........- 219-220 | Bell, Robert, on rocks of Hudson Bay.... 122
oS. W. Powell, on POOR OR ne cccclkcbck> x 220-221 | Bennington, Vermont, section............ 276
«GK. Gilbert, on rocks of ............ 220 | Big Cottonwood Cajfion, Utah, section... .157-158,
_ + A.B, Marvine, on rocks of.......-..-. 220-221 159-160
2 C. A. White, on fossils of....... : ats, 221 | Big Horn Mountain range, Montana, sec-
a ‘ C.D. Walcott, on rocks of............ 221 ID odacdcthigshdwciend anllosescaees <a 325-326
Sh. SE 2 235 | Bigsby, J.J., on rocks near Quebec ...... 114
- problems for investigation in ........ 385 on Montmorenci Falls .....--..-..... 116
on Atlantic Coast province, definition of.... 50, 253 on rocks of the St. Lawrence ........ 116
Vos Cambrian rocks of .......-........-.- 50-78 on Lake Superior sanastone ......... 188, 252
een paleontology of -....-....-......,..-. 78-90 on Potsdam, of New York ...... geese 206
-——s summary of knowledge of Cambrian correlations Of .J.........6.-2e.sse- 395-396
me." RN Cadi setisthis 6b dae a hv 5 253-274 comparison of rocks of New York
< sediments of ..-..- CE A SE 358 ee CER DemeE aoe”: ALNa 418-419
A fauna of..-...-..--.-2200--00eseeeeee 370 | Billings, E., on red sandrock ......-...... 97
th physical characters of strata ........ 273-274 on Georgia slate ........-.+2-.-..00.. 102
Bs: - Atlantic Coast and Rocky Mountain on Winooski marble.........-...--.. 103-104
a ae Ee ee aoe 386-387 on Point Levis fossils......... 116-117, 150, 151
‘' “Atlantic Coast series, J. W. Dawson on.. 56 on correlation of faunas .....-..--... 150
3 x Atlantic Coast series of America and on fossils from Potsdam group of
‘4 EE ec DL ashes cnlse ine sect 373, 374-375 Catan tbh ay dose beta Sen ss eee 150
435

ee ee ae ee i ee a ae

436

Page
Billings, E.—Continued.
on fossiJs from red sandrock.....--.-. 150
on fossils in correlation.........----- 406-407
Black Hills, Dakota, E. James on rocks of 214
H. Engelmann on rocks of..-.-.------- 214
Meek & Hayden, on rocks of.-.-..---. 215
¥F. V. Hayden, on rocks of..-.-.-----. 215-216
N. H. Winchell,on rocks of......---.. 216
R. P. Whitfield, on fossils of -..-...-.. 216
H. Newton, on rocks of.......--..---- 216
Hw, B. Oarpenter on |... asectevonnues 216
GS Gh. bes - be wecdoadas sean ee 233, 234, 348
TOGIS Of 3. co | anaes op pee anes eee ee 347-349
Bohemia, Cambrian rocks of ....-...---.- 275
Bonne Bay, Newfoundland, section -...51, 255-256
foanile from 2.20 cepenerdenewse teases 256
Boston and vicinity, J. W. Wobwiss on
TOCKS ‘Of; cnndic toons eeeeaee sea 72
EK. Hitchcock, on rocks of ......-.-..-- 73-75
Bow River series ....-....-..-..-. 2---164, 326-327
Bradley F. H., on rocks of North Caro-
SiS 3 ood 2 eo pel gatatie anaes « 138-139 -
classification of ..... Set oa eee 143-144
, onrocks of Utah ........-..-.--.---- 156, 157
on rocks of Idaho ..vc...ceceucws sce 161
on rocks of Wyoming..:.....-.-.-.-- 212
on fossils from the Adirondacks...... 231
correlations Wy 2.c 2. 8o8 Sfve ssp awac ob 411-412
Braintree, Massachusetts, L. oes MR on
poeks at 2. Uwe euos sce ct ao eeeteyld 74
W. B. Rogers, on rocks at.......--.-- 73, 74
I. Lea, 0n TOGKS Gb. 1-200 os. ected ects : 74
C. T. Jackson, on rocks at............ 74
J. Barrande, on fossils from.......... 75, 88-89
N.S. Shaler, on rocks at........-.. x ok 75
T.S. Hunt, onreeks at... ccccsven--2. | | 75-76
W. W. Dodge, on rocks at, cited...... 75
W. O. Crosby, on rocks at ............ 76, 77-78
J.Green, on fossils from .......---... 88
W. B. Rogers, on fossils from......-.- 88
C. T. Jackson, on fossils from ........ 89
A. Ordway, on fossils from..........- 89
W. W. Dodge, on fossils from .-....... 89
R. P. Whitfield, on fossils from...... : 89
C. D. Walcott, on fossils from ...--..-. 89
Braintree quarry, Massachusetts, : E.
WuGaworth, ORislctecika fone verieens 271
Bretonian, definition of ..............---- 247
Brigus, Newfoundland, fossils of......... 55
Brigus Head, Newfoundland, section. -... 260
British Columbia, G. M. Dawson on rocks
eo atid et we ae “ae en 163, 164, 165
R. G. McConnell on rocks of ...-..... 164
Broadhead, G. C.,on rocks of Missouri. . .200-201,
j 340-341
Brogger, W. C., on Prospect Mountain
POND 2 nar ka coees ones ee ccmeenee. 314
Brooks and Pumpelly,on Lake Superior
Sandstone 22 esoew ne ees fue edd, ek 196
Buckley, 8. B., on rocks of Texas........ 218
Burnet County, Texas, section............ 354-355
C.
Calciferous sandrock in Wisconsin. ...... 172, 177
Calvin, S., on well at Washington, Iowa... 188

: Bone OL,

Cambrian continent.........- Tes 3€4-365, 386
Cambrian faunas, order of succession of, A 3h
in Amofiog. 22. {oA 2 ee 861 3
Cambrian, base of.....- J gisbnt adnan 362 a
sedimentation of...... ......-. 362-363, 363-369 |

Sammit of! .2.2..0.acetewuseanteeee 362-363

faunas of... .). ve. ssenteleaeceeean 369

subdivision of.... ......... ee Seas oe 370-373 ©

sediments of..... LieSue eh tbat retype 385-3. 86

Minit Of... cc3 3c ee ee 388-389 4
Cambrian time, geographic areas in... -49, 368-369
Cambrian group, delimitation of..... alpen 17° ‘

divisions of... 2.0... cea eee 49, 389-390

A. RB. O. Selwyn ‘ition ci cae oe 119
definition of, by Sedgwick and Mur- tis
chison;))3.; 0.0. 7c0 22008) «eee 237-239..."

divisions of, by A. Sedgwick ......... | 39

use. éf in America ..05. 35. Sst 241 Ke

where separated from Silurian..-.. . 241, 363

sediments of in eastern Massachu- a

Fe ee ep. oy 12
aynopeis of. '... Jon bevarwdeaeeeenne co eum
formations Of: . 2.202 hak tack eee 359-360 oe

Cambrian and Taconic, T.S. Hunt on..-. 108» <.s.

OBO GE t odds ses gurd coat dene eee a
Cambric, used by P. Frazer.....;..-...-.. 131
Camp Baker, Little Belt Mountains (Mon- yy

tana) section........ .......------ 325
Campbell, J., Nova Scotia gold field ...... ane
Campbell, H. D.,on rocks in Virginia.... 187 oa
Campbell, J. L., on rocks of Virginia.....- 135,136
Campbell, J. L. and H. D., on rocks of Vir- ahh A,

iD. ene fe Hon has gee oe RS
Canada, geologic map of...-...---.----. 59,119-120,

’ -W.E. Logan, on rocks of .--.......... 207-208 Th

Alexander Murray, on rocks of...... ae E

problems for investigation in.... .... 382 aa
Canada Bay, Newfoundland, section... 257, 273.
Canadian extension of the northern Appa- ‘ae

lachian district, Cambrian rocks _ ;

pe SEMORS aid oR LI aT 8, 114-122, 285-287
Canadian extension of Adirondack sub- SR, ny

province, Cambrian rocks of...... 207-208
Canadian extension of Rocky Mountain " 2

province, Cambrian rocks of..... 326-327
Canadian extension of upper Mississippi bs!

province, Cambrian rocks of..-.- 334
Cape Breton, G. F. Matthew, on rocks of. 55

H. Fletcher on rocks of..-......... 63, 266-267 —

G. F. Matthew, on fauna of.......... 65, 84
Caradoc sandstone, position of.........- 239
Carpenter, F. R., on Black Hills..... 216, 348-349
Castle Mountain group...........--. 164, 326, 327
Chamberlin, T. C.,on Potsdam sandstone

of Wisconaiti 2-22... <us3n-ennsee 9)

work of, in Wisconsin ............. 179, 180 |

on Lake Superior sandstone. ..... 198, 338, 339

on fossils from Wisconsin ....... 226, 227-228

Chapman, E. J., on Climactichnites..... fr 4
Chateaugay Chasm, New York, section... 342-343

Cherokee slates described ............... 138
Chester, F. D., on Potsdam of Delaware... 123
Chikis quartzite, P. Frazer on ...-- Ay. 129”
description of.......----------+-----+ 288,289
t

Chilhowee, definition of........-..-.. ye

* 3 eo peat Cana 3s te 7r N itn! , ; hse ig ©
m 7 ’ r ;
Ne ae ae INDEX. 437
Bi Page. Page.
chinowse sandstone, J. M. Safford on... 300-301 | Dana, J. D.—Continued. )
"Sani Cambrian rocks of................ 377-378 on A, Wing's discoveries in Vermont 107
Cambrian fauna of...............---- 377-378 quartzites of eastern New York ..... 109
f - Choceolocco MNEs oe Lacu ces ¢ tetas « 247 principles of correlations ............ 407-408
| Clarksburg Mountain, Masonstisitin, Dana, J. F.and 8, L.,0n rocks of eastern
Bye ON GE an SES SSN a pe 275-276 Massachusetts................... 72
ee Classification, IIE 3 a's 0h asa Seam cg 17 | Dana and Grinnell on rocks of Little Belt
_ Clemson, T.G., sections in Virginia...... 133 Mountains, Montana ............ 162
Colorado, Cambrian rocks of.... 209-210, 351-354 | Daniels, Edward, fossils from Black River,
' F.V. Hayden on rocks of.........--. 209 Wiscoiistn .J4.vaeev eens a2. 2 223
Ay ~AS G. Peale on rocks of.............. 209-210 | Dawson, G. M., classification of the Cam-
Ot ‘Arnold Hague on rocks of.......--.. 210 brian in Canada.................. 67, 123
= $F. Emmons on rocks of .........-- 210 on rocks of British Columbia ..... 163-164, 165
, fossils from Quandary Creek, in...... 210, 234 on Selkirk range, British Columbia. -. 165
for, i synopsis of Potsdam rocks of....... 353 | Dawson, J. W., on Atlantic coast series... 56, 59
4 : bo problems for investigations in..... Se 384 Nova Scotia metamorphic slate .....- OV
Colorado River section...........--.---.- 220 on rocks of New Brunswick ....._-. j 60
at ‘ Comstock, T. B., on rocks of Wyoming... 212-213 on strata at St. John, New Brunswick 61
* division of Cambrian of Texas ... 219, 355-356 on Acadian series ........... ..2..222 62
aad definition of Katemcy.........-.----- 246 on fossil tracks from Canada......... 231
i SS . 246 om Caerleon ce as ccsomung sa sbee 241
NOME TOMOFy..-......-.-..-..-.....-4.- 246 definition of Acadian ................ 248
7 y on rocks of Wind Mountains....... 349 | Delaware, F. D. Chester on Potsdam of... 123, 288
my ag definition of.............-.- 246 | De la Beche, on use of organic remains... 398
Be Conrad, — T, A., formations of New Devine, T., trilobites of Point Levi ..._.. 151
oe | Yee ee 203, 204,205 | Dewey, Chester, work of, in Massachu
Bo on fossils of Adirondacks ............ 229 BOGS . 2... 2. eee eee ee eee 93-93
son. use of fossils in correlations ....... 399-401 | Diamond Creek, Arizona, section ........ 219
Cook, G. H., on Potsdam in New Jersey.. 122-123 | Dikellocephalon ................-..------ 222
-___ 9n Green Pond Mountain rocks...... 123 | Dodge, W. W.., on fossils from Braintree - 89
Bai” Coosa, definition of......... .....2..-..-.- 247 on rocks at Braintree, cited .......... 15
Coosa shales, fossils from............-.--. 305 | Dutchess County, New York, Mather,
a 308 Smock, and Dwight on rocks of.. 111-112
Coosa Valley, Alabama, rocks of ......... 308 granular quartz in ..........--....0.. 276
a Cornwall iron mines, T.S. Hunt on.....-. 127 TOCKS Of... o-oo sein en nawe onsnnin'e 283-284
_- Correlation of North American and Brit- Dutton, C. A., on Tonto of Arizona ...-.. 221
Bw eee -........--.. “fh eps 417-418 | Dwight, W.B.,on the rocks of Dutchess
m Correlation, methods of ,..........-....-. 421-434 County, New York ..........2... 111
wa _ superposition in...................... 421-499 fossils from Poughkeepsie, New York 153
er. ha use of organic remains in ........-... 422-498 on rocks of New York................ 283-284
Se an dite somes in............. Fane ta tune oan 424-425 E
stage of evolution in................. 425-426
a SS 426-427 | Eastern border or Adirondack sub-proy-
__—-— contemporaneity and homotaxis in... 427 ince, definition of................ 201.
ia percentage of species in ............. 428 Cambrian rocks of -......-.......---. 201-208
“We lithologic character in ............... 428-499 | Eastern sandstone, description of ..... 197, 335-336
My Ae unconformity in......... . oe eee 429-432 definition of............-..-......-... 253
i a) nomegeny in............. 5 ie eR 432-433 | Eaton, Amos, nomenclature of........... 92-93
eS. "topographic features in ............-. 434 on rocks of Vermont......... oy Pee , 98
a { Crosby, W. O., on rocks at Frenchman’s definition of granular quartz......... 260
a a 8 eee ee ee 68-69 correlations of... ........-......... 392-395, 399
__- on rocks at Braintree, Massachusetts .76, 77-78 on use of organic remains ........... 394
on Cambrian rocks of eastern Massa- East Rutland, Vermont, limestones of --. 276
Ge “as Sp pian 268-270 | Elliott, J. B., on rocks of Tennessee..... . 144
-——s on rocks of Nahant........... hie 2 271 | Ells, R. W., on Cambrian rocks of proy-
1 Ne yo a Oe ape eed 120 121
; D. on rocks near Quebec. .-.............. 285-286
« Emmetsburg, Iowa, section ...........-.- 187
> Dakota, Cambrian rocks of......-. 214-216, 347-349 | Emmons, E., classification of .-.......... 94, 403
4 Dale, T Nelson, work of,in Vermont..... 283 on granular quartz .............s---- 94-95
y* Dames, W., on fauna of Cambrian of (it TAG BADATOGK, 5. «5.0 0'<ns nas ain anne « 96
‘a és ae IE 6s en ood ad beled ay awn 377 on Taconic system ..........eccces« Mu 98
¥ Bc Dana, J. D., on granular quartz of Massa- on Montmorenci Falls ............-..- 114
EE 106-107 fossils of Taconic system ...........- 148-149
om red sandrock ............-.-...--- on Potsdam sandstone. - ..202-203, 204, 205, 206

107

438 é INDEX. |
Page, —
Emmons, E .—Continued, Georgia—Continued, Say!
on fossils of Adirondacks............ 229, 231. Cambrian rocks of ..... ( «+++ 144-146, 303-305 Ss
on Cambrian in America ........---- 240 G. Little on rocks of .........-..--..- 5 ,
definition of Taconic ..............-.-. 242-243 J. T. Henderson on rocks of......... 145 hie
definition of Potsdam........... oe 244 A. R. McCutchen on rocks epee ets 145-146 OR
Emmons, S. F., Big Cottonwood Caion paleontology of .<-2.>... 2c 1 sckeseeen = 158 << 3
section .............-------.----- 157-158 | Georgia and Alabama, problems for inves- |
tabulation of rocks of Colorado...... 210 tigation fn... 42k oe rs
: on rocks of Colorado. ...cavecmenncane 351-352 | Georgia, Vermont, C. D. Walcott on Le ake eT
Endtich, F. M., on rocks of Wyoming.... 213 Cambrian of)... i.<.ccneenedenkeee 0 cf
Engelmann, H., on rocks of Black Hills... 214 Wotton ab. 322. ). 72 ere 277, 278, 279, 280, 981 ee
English and American classifications com- Georgia formation, definition of.......... 240, 250 %
MOTOR | ii» oc x Sen <i cee 376 J. Barrande on fossils of............- ggg 2 er
Estoria, Cambrian rocks of .......-....- mek 375 | Georgia group, C. H. Hitchcock on...... 101742
Etheridge, R., on Cambrian of Australia. 378-379 | Georgian, formations correlated with. -.. 360 ;
Eureka District, Nevada, fossils from.... 167-169 | Georgia slates, description of ............ 98-113 a
section........- mea aioeke aig cael dnaintae 313 Hi. Billings ‘on,..2.2 0, <4, .cueseseabtene 102
J. Marcow 0B. 3.0% dand anon ence ann Sa 103
F. C. H. Hitchcock on....-si5.casecs es 106, "4
character of..... GS west eats Tee 2B
Fall River, Massachusetts, W. B. Rogers, Gesner, A., on rocks of New Brunswick.. 59°?
on rocks at. ...- 2.000 -2--s0sennon 75 on rocks of Nova Scotia.............. 662.4
Ferrier, W.F., on fossil track from Adi- Gilbert, G. K., work of in Nevada........ 156” Mi
rondacks -.....- eee tenn nen n-ne 232 on rocks of Arizona........2-4- secs 220
Fitch, Asa, on Taconic slate and sand- definition of , Tonto 2.%20...cccleece ee 245
BUONO .......-----eweenncnnncencee 98-99 correlations by... <<. <2s¢2- /2 ese ae 412 =
on fossils of New York.........-. 148, 149-150 on topographic features in correla- i 7 a
Fletcher, H., on rocks of Cape Breton. .63, 266-267 tien . 2.4. oe eee ia 5
Foerste, A. F., on rocks ot Nahant, Massa- Grand Caiion, Arizona, section .......... * 563
chusetts wee renee teen enn n ne 78 | Granular quartz, description of.......... 91-96 :
on fossils from Nahant, Massachu- E. Wathons on....: 2222-2 94,95
BOttS .-..---2.-2n-s 2 seenee--ne eens 90 S. WSil oes Oo “aie avenee 1D: a
on rocks of eastern Massachusetts. - . 271 ©. H. Hiteheock om) o25 2: oos «fcc eeee 108° 8
Fontaine, W. M., on rocks of Virginia.... J. D-Dahs 00:).03- 2 See - 106,107
135-137, 291-292-297 C.D. Walcott on .........2--02- Pe 3
Ford, S.W., on rocks at Troy, New York. 106 N, H. Winchell 6niv3 32. ee 186, 187 Sy
tossils from Troy, New York ........ 152 defnitida of?<c. <o eae ae 250
Foster and Whitney, on Lake Superior age of.....- OSs Fre Py Sek 250
sandstone........ wrneee weeeeee 191-192, 193 distribution of .................-. 275, 276, 372
table of rocks .......---...---- o-seeee 192 characters of s.o25.22- Case. cece 275-277
France, Cambrian rocks of............-.. 375 | Great Bell Isle, Newfoundland, fossils
Frazer, P.,on South Mountain rocks..... 128 OP ot ere ene eee 153, 259, 261°
on Chikis quartzite..... at tae tesieoas 129 section: 22.22 eer eee 258, 259
primal quartzites...-....-.-----.---- 129 | Green, Jacob, on Paradoxides...........- 88
on Hellam quartzite or Potsdam sand- Green Pond Mountain rocks, G. H. Cook see
REPOS J. say ta on oe eee aan owen se 131 one: 2: ere RK el oe 123 —
on rocks of Pennsylvania............ 289 ;
Frenchman’s Bay, Maine, W. O. Crosby H.
OH TOCKS'Ol:--speernecas a Se Sot 68-69
Hague, Axnold, on rocks of Nevada ..158, 159, 160
G. on rocks of Colorado ........--..--..- 210
on the age of rocks of Laramie Hill,
Gallatin City, Montana, section.......... 162 Wyoming {227223 se Pls 212, 350 |
Gallatin River, Montana, section..... 162-163, 324 definition of Hamburg ........-...--- 246 —
fat. er Ce ee . 325 definition of Secret Cafion........... 246
Gaspé peninsula, A. P. Low on rocks of.. 120 definition of Prospect..... bin Swe cookie 252
Geiger and Keith on rocks at Harper’s Hall, C. E., on hydromica slates ........-. 129
Werry ...cpeseens oatoceie AB 137, 138, 291-292 on Potsdam ef New York........ asen 207 ©
Geikie, A., on Cambrian rocks of Scotland. 376 | Hall, James, on fossils near Troy. eee - 99
on Cambrian rocks of Ireland........ 377 on granular quartz. .........-2ceesese 100
Geographic areas in Cambrian time. -..49, 368-369 on fossils of Vermont ...-.. oa inns babe ay SCE
Geologic classification..........---.--.--- 47 on fossils of New York....... eee ORE ME GS
Geologic nomenclature, general considera- on fossils from red sandrock......-... 149
TIONS ‘GA. As Sieian's bn eh aetna 236-237 on fossils of Hudson River group.... 149
Georgia, G. White on rocks of..... eae wes 244, 145 on fossils of Quebec group ......-..-- (149°

ge INDEX. 439
ie ; “ he
an Page. | Page.

v ‘Hall, James—Continued. parenerek, C. H.—Continued.

Olenellus proposed by.....-..-..- | on red sandrock............... wat nae oth» IOG
- onrocks of Wisconsin ...-.-...--. 173, 175-178 on Cambrian of Vermont............. 107
on age of sandstone of Wisconsin and on sections in Vermont and New
Lake Superior .......-...-- eo ee 178 TINUE ee ne owen ne obec ecdnae 108
on Potsdam of Iowa........---------- 187 fossils of Potsdam group............. 223
on Potsdam sandstone of New York . 205 proposes Potsdamic.................. 252
on fossils of Wisconsin... -222, 223, 224, 225, 226 on mica-schist series of New Hamp-
fossils of Adirondacks ............--- 229, 232 ahire. 2 Cee 268
on names of formations ..-.......---- 401 | Hitchcock, E., on rocks at Attleborough,
on use of fossils in correlation. .....-. 401-403 Massachusetis ....-....5--.2.---; 73
_ methods of correlation...........---- 408, 409 on rocks of Boston and vicinity...... 73, 75
principles of correlation ..........-.. 415,416 | Hiawassee River, rocks of...........-..-- 141
North America and European forma- Homogeny, W. J. McGee on .......-....-- 432, 433
tions compared by .......-.--..-. 416 | Homotaxis, T. H. Huxley on...........--. 427
‘Hall and Whitfield on fossils of Ne- Hough, F. B., on Potsdam of New York .. 205, 206
: vada ....... 8 EEL 159, 166,167 | Houghton, Douglass, on Lake Superior
on fossils from Adirondacks ......... 231 BENdStONG.. 2065 isc dev soneeeceee 188-190
_ Hamburg, definition of-.............--... 246 table of rocks of Michigan Reet. 189
Hamburg limestone and shale, description Howell, E. E., on rocks of Nevada........ 156
‘A> Deanne ksccnc conadetcnes-«« SID-SLE Wireless. Tan rocks of Newfoundland ... 53
— —s—s—is«séfatana Of... 2. 0-22-22 e ene eee ee eee 316, 3i7 | Hudson’s Bay, Cambrian rocks on ......- 121, 122 |
Harper’s Ferry, Virginia, Geiger and Hunt, T. S., on rocks at Attleborough,
; Keith on rocks of ...........--.-- 137, 138 Maasachusetts .....)-. nc céduase 73
a oe ee 291, 292 on rocks at Braintree, Massachusetts. 75-76
Hartt, C.F., on St. J sie group... .-...-... 62 on geology of Vermont............... 104
_ Hayden, F. V., on rocks of Montana...... 162 on Cambrian and Taconic............ 108
_on rocks of Colorado. -....-...--.----- 209 classification in Canada ...........-... 120
on rocks of Wyoming........--.-.--. 211, 212 on Cornwall iron mines, Pennsylvania 127
. on rocks of Black Hills .......-....-. 215, 216 on Auroral limestune ............-.-- 127, 128
____ Hayes, C. W., definition of Connasauga. . 246 correlations. 6f is 5scn<a's 4 ieS* aamnnes « 132, 414
- -——ss definition of Rome sandstone .....-.. 247 ou Potsdam of Pennsylvania......... 132
Re definition of Weisner.-.-...-......... 251 on Scolithus linearis ...........- hese 3 132
B _ Section in Georgia ......... a sseeeeee- 304, 305 on Lake Superior sandstone ...... 195, 197, 198
* ‘Hellam quartzite ......---..-----.------- 131 on Potsdam of New York ............ 206
_ Hemmingford, Canada, section.......-... 343 on Cambrian, cited ..2......2.<. neces 240
a Koi Henderson, J. T., on rocks of Georgia.... 145, 303 OGL 2 MNS on paciis ocd espana tee 243
i Hickory, definition of........2-.202+.0-. 246 | Huxley, T. H., on homotaxis...... .....-. 427
- Hicks, H.,on Tremadoc group........... 242 | Hyatt, A., on fossils of Straits of Belle Isle 54
Se -. on sediments of the Cambrian..... da 373 on sife history in correlation ......... 426
--—s on Cambrian of America and Wales. 375 | Hydromica slates, C. E. Hall on ........-. 129
'. __ _-Highgate Springs, Vermont, section...... 279
pais! Highland range, Nevada, fossils from .... 171 t)
Bi section....... RES eee 317, 318
hey eo ak stank coco - 318,319 | Idaho, O. St. John on rocks of.........--- 161
Ss Hind, H. Y.,on Waverly gold district. -.. 57 F. H. Bradley on rocks of..........-.. 161
wg on gold-bearing rocks of Nova Scotia. 58 A.C. Peale on rocks of -..........--.. 161
a a » on gneissoid series of Nova Scotia ..-. 58 Cambrian rocks of............ 161, 162, 320-323
Be : Hitchcock, C. H., on Mount Desert, Maine 68 Lower Paleozoic section ............. 323,
oe on rocks ious Portland, Maine-..... 68 Sedimentation of 3. . 425 kl beac ae 328, 329
on rocks of Maine..................<. 69 | India, Cambrian rocks of................. 7 ae
classification of rocks in New Hamp- d’Invilliers, on Potsdam sandstone of
ad tow as de dcedebuneavenen- 70, 71 Poenpsylvania y\. <'s\0~c icin agerrced 130
on classification of rocks in New Eng- on correlation of the Potsdam........ 404
eS Ne Can aide wats ae sb adac'nt ae 72 | Interior Continental Province, definition
on Georgia group ................- 101, 249, 250 ene ee EEE Pee Fe ae 171, 330
on the name Georgia.......-..-.-...- 106 Cambrian rocks of ..........-. 171-221, 330-347
on rocks of Waterville, Maine........ 101 SOGIMMIGHUS OL 2222 Skea cd ccncaweene nse 358
on guartz rock of Vermont..... pret ide 96 TAUBA. OFS. sia 20's Ns Hoeneta cia cad pewun on 371
on fossils from Vermont ..... ae she Siu 99 | Iowa, Cambrian rocks of ............-.... 187-188
on formations of Vermont......-... ae 164 | Ireland, Cambrian rocks of...........--.- 377
- on Potsdam in Vermont.........--... 105 | Irving, R. D., on rocks of Wisconsin..... 178-179
On Winooski marble .....-..........- 105 on Cambrian and pre.Cambrian for-
106 mations cited ..... Jondaan ben keene 181

on granular quartz. ..........-...----

440

a at OSE aN RNC St ein OR coe
cy ere ee Lae hy ve aah a, Witkin: o Rasy ye NY i.
| INDEX. ty R50 RO ee ee
iy , ey ' ae ye ,
’ Page. Page. vee
Irving, R. D.—Continued. Lake Superior sandstone—Continned, VASE Bee a
on Lake Superior sandstone... . -- 196-197, 198, D. D. Owen on.......... eee hes. Ipdagy «38
199, 335-336 age of bactiabhagicea Stns 191, 192,194,197
definition of Madison.........------- 245 CL. Jackadn'od . SN Ae 191, 193
of Mendota........---- gah 245 Foster and Whitney on...........191-192, 193
of Eastern and Western J. W. Foster on {.. .w-..€.2gepecmueeeee 191
‘ sandstone ..........----- 252 Bela Hubbard on ...............- -.---191-192
on lithologic character in correlation. 428 Jules Marcouon.........- pastenennene ail thee gp
on unconformities in correlation -. --. 429-432 J.D. Whitney on...) ...-.02.022: ~-+---194, 198
Irving and Chamberlin on Lake Superior H. R. Schoolcraft on..-..........- aie ace ae) CL
SMBGAEORG 22> - ck icane es’ ekpeatees 199 A. Winchéll og -. .....::20 2 ios tapewacede eee
q..8: Newberry ons... Soon nceeeate 194
J. yO. SLO OR. kee 195, 197,198
we Charles Whittlesey on...............-. 195 ;
Jackson, C. T., on trilobite from New- correlated with St. Croix.....-.-....... 195
foundland.........--- iS Se - Thomas Macfarlane on........-... danas} oie
on rocks of New Hampshire .....-..- Ll Alexander Agassiz on..........-..0---- 195
on rocks at Braintree, Massachusetts. 74 Brockiand: Paeal ;
; : pelly Qn: 25k. 2. ane ee ee
on fossils from Braintree, Massachu- C. Réwiinger on -.5.2.. Lea - 196
SEED = aa eee eee wa R. D. Irving on..........-.22.. 196, 197, 198, 199
on red sandrock Pi IG 7 le 4 ee os E. T. Sweet on -2202% 5... ieee 196-197
on Lake Superior sandstone ..-...---. 191-193 WE H. Wadswotth on 197. 198
James, Edwin, on Ozark Mountaina, Mis- ae Ca af ide ilo Behan ad A bee
: at , j 199 A. R.C. Selwyn on .... 2.0.0... ccee -.--197-198
on Black Hills, Dakota sosoee--. 218 fo et windlall an. o
correlations of ...-..--.------+-.+---- 896-397 T. C. Chamberlin on.........-. oe tee 198
Jenney, W.P., on rocks of Texas.......- 218 M. EB Wedevorth off! ee ey 198
Johannian, detinttice Gus Jae Sdn ak 249 Irving and Chamberlin on.....c...ca-. 199
Johnston, J. F. W., on rocks of New foanile Of 3... bee eee
Branswick...-......-------+--4-- 60 definition of.....:....... Pe, ee we a see 252
Jukes, 7.5. on rocks of sidnlidabipa poe ata 50, 51 Lake Superior section ... .. = ee ee ao 336-337
definition of St. John RU es? ite? Je yh 248 Lane, A.C., ou rocks at Nahant, Massa-
Jukes-Brown, A. J., cited on Tremadoc chusctta, cited C2200. : 28
BIALCS «-- 2-02 -naw Be pin Ada) wa 241 Lapham, I. A., on rocks of Wisconsin. ... 172
K Laramie Mountains, Wyoming, age of J
Z Cambrian rocks of ..............- 212, 350
Kanab Creek, Arizona, section........ a 356 | Laughing White Fish River, Michigan, ae
Katemcy, definition of...............-.... 246 section....---. peek eter Fh ict p< 337-338)
Kayser, E., on primordial fossils of South Lea, I., on rocks at Braintree, Massachu- vi
AUTOR) ads. (actincth abeed ns 30. 379 setts .--..--.----------- Naor tk 1 eee
Kelly’s Island, Newfoundland, section.... 259 |. Lesley, J. P., on South Mountain rocks... 127 “
Kerr, W. C., on rocks of North Carolina. 138-139 on Primal series ---........--.------. 129-130 +a
Kicking Horse Pass, fossils from. ......-- 163, 170 atlas of Pennsylvania............. se 1ST) ss ae
King, Clarence, on rocks of Utah ........ 157 work of, in Tennessee -.....-.. repens Aa
comparison of Utah and Welsh rocks. 157 on rocks of Pennsylvania............ 268-289
on rorks of Nevada and Utah......... 159-169 | Levis shales described ..-....- here aden 285-286
correlation by.....-.----.---------s-- 412 | Lewis, H.C., on primal slates and Pots- 54
King, H., on rocks of Missouri.........-- 199 dam sandstone ...-......--------. 131
correlations by.....-.--.-.------------ 199 | Lingulella lamborni .....-........ 200-201, 340, 341 '
Knox sandstone and shale, description of. 301-302 Little Belle Isle, Newfoundland, section. ‘250° >" 4
Souda Ga: 52 oc. se ee 302-303 | Little, George, on rocks of Georgia ......- 145
Knox sandstone of Alabama............. 306-307 Llano County, Texas, section ..-......--. 355
Knox shale of Georgia........--...--. mt 3093 | Logan, W. E., on rocks of Newfoundland. 51 *
Knox shales of Alabama................. 307 tabulation of Lower Paleozoic rocks. 51, 52
Kootanie Pass, section ..........-....--. 163 on rocks of Lower St. Lawrence. .115, 118-119 x
on rocks of Quebec..-..-.---.+------- 116 4.4
rs on Quebec group... .......-.--.------ , ivy
on rocks of Canada........... Py hehe 207-208
Labrador, Lower Cambrian in ............- 274 on fossils of Canada.........-..--- 229-230, 231
Lake Superior sandstone, description of. 188-199, on Scolithus linearis ........2..-...-- 230
335-339 distribution of Trenton Jimestone ... 405-406 |
Cid. BigsDy. Ow ide '-\ qv n'a eaieebmenx ae 188 | Logan and Billings, on the rocks of the . * 2
H.W Bayfield On. J> uct. cela ebare = 188 St. Lawrence River ......-..-..--. 406
Douglass Houghton on.............-.. 188-190 | Low, A.P., on rocks of Gaspé peninsula.. ” 120 a
HW. D. Rogers OD.2....c.c0ctoseceven= ke 190 on rocks of Lake Mistassini......... 12200

\
Page.

239

Lower Cambrian fossils in Bristol County,
: ' Massachusetts................... 271-273
ert) Lower Paleozoic rocks, W. E. Logan’s

oe. 4} Pebalation of .........-.-..0<2-.- 51, 52
__— Lyell, Charles, on Potsdam of New York. 205
ae : Lyman, B.S., on rocks of Virginia ...-.-- 134
Pate” M.

Macfarlane, Thomas, on Lake Superior
—_ a SS 195
Maclure, William, on Appalachian rocks 91
% Goprensiens Of -2........--.-....-2-.- 391-392
2: classification of rocks .........-.....- 392

‘ nad Madison sandstone, definition of......-.. 245, 331

Madison, Wisconsin, section............- 332
Maine, Cambrian rocks of .............- 68-69, 267

___ Maine and New Hampshire, problems for

; x investigation. -.-.. Ren eete edwards 381
__ Malade City, Idaho, fossils of ..........-. 320-321

Mh Manuel’s Brook, Newfoundland, section. 52, 260-

‘oe 261, 262, 273

_-—- Manitounuck group......... en eee 122

re “ar J., on Georgia slates .........-.- 103
43 on red sandrock - et OF seas ee 103

vex on Taconic of Lake Champlain ...--. 108

Re on strata of Taconic system .... -.--- 109, 110

--——s on classification of Taconic system .. 112, 113
Seis) on age of Lake Superior sandstone .. 192

; rad proposes Georgia ...... ........-..... 249

*, proposes St. Albans .........-......- 281
| Marsh, O.C., on fossil track from Adiron-

4 0 ee eee 231

‘ _ Marvine, A. R., on rocks of Arizona...... 220, 221

__-- Maryland, Primal series in .............. 133

ep po@amurian rocksof ..................- 289, 230

Massachusetts (eastern), J. F. and S. L.

Bs tw ‘ae, On rocks Of................ 72

* _ Cambrian rocks of..........72-78, 268-273, 274

“Sia M. E. Wadsworth on rocks of........ 76, 77

Be MIMI aisles oo oe ne anna nn noone 88-90
Bhat work of C. Dewey in .... .... Rapa 93, 94

4 problems for investigation in ......-. 381

c Mather, W. W., classification of ......... 95

-———-.on the rocks of Dutchess county,

E> PUEMWE Saoanndocensagenness. 111

7 ‘on Potsdam sandstone of New York. 204, 205

a ‘Matthew, G. F., rocks of Cape Breton and

a Newfoundland........---.--...-- 55

_-—s—s elassifications of rocks of New Bruns-

at IMIR ir ii cn. caventnnn wane nda. : 61

>a on rocks of New Brunswick ......-.. 62, 64

et on rocks of St. John ............... -- 64,65

iy oan on fauna of Cape Breton ...........-. 65, 84
on on pre-Paradoxides zone at St. John .65, 67, 86

A Be ry classification of the Cambrian ....... 66, 67

re definition of Bretonian ...... ........ 247

Pe) definition of St, John ................ 249

_—~—s definition of Johannian .......-...... 249
on St. John BERS Pc clk ie, 263, 264, 266

-—s eilassification of rocks in Acadia ..... 265, 266

f a -\ eomparison and correlation of rocks

veg of America and Europe .......--. 420, 421

AS |

By hase -

a Vr

INDEX.

Page.
Matthew and Bailey, on St. John group._ 62
McConnell, R.G., work of in British Co-
I oo tin 0 aiwin e sdadn samen 164
McCreath, A., rocks of Virginia.......... 135

McCutchen, A. R., on rocks of Georgia. 145-146, 304
McGee, W. J., on homogeny in correla-

Was! oo 5 9 Ne 432, 433

Meads, A. D., section at Stillwater, Min-
nesta, in Well ic. 2222-5. .2 45 186

Meek, F. B., fossils from Antelope Spring,
OVER... cna tkaeeren secete wasn’ 155, 165
on fossils from Idaho ........-.-.-..., 165
fossils from Utall’.< 401 seuscwoten sane 166
on rocks of Missouri ...........--.--. 200, 339
ou fossils in correlation........-..... 410, 411
Meek and Hayden,on rocks of Black Hills. 215
fossils from Black Hille.............. 233
Mendota limestone, definition of ........- — 245
GEROri PION: OF... «co avncnwnmagedstemies 331-332
Mica-schist series, C. H. Hitchcock on... 268

Middle Cambrian in Atlantic Coast prov-
WE Son do kine innit ae 274
Milne, J., on rocks of Newfoundland... - 54
Minneapolis, Minnesota, section in well. - 184
Minnesota, D. D. Owen on rocks of......- 181
Cantbriah rocks Of . «505% sjaeaqeean 181-187
« N.H. Winchell on rocks of........... 181-187
general sectior in ..............-.---- 334
Missouri, E. James on rocks of........... 199
H. Kimg om rocks of . .- one <--<¢ deaane 199
G. C. Swallow on rocks of...........- 199 200
Cambrian rocks of ...........- 199-201, 339-341
3B; Meek on rocks of 22. ....ccncon ae 200
GORI Oey nna saan oo's thiein'n both bee ‘ 229
G. C. Broadhead on rocks of.......... 200, 201
generalized section in .........--..... 340, 341
problems for investigation in ........ 385
Mistassini Lake, A. P. Low on rocks of.-. 122

Montana, Dana and Grinnell on rocks of. 162

F. V. Hayden on rocks of ............ 162
Cambrian rocks of ............ 162, 163, 323-326
Montevallo shales, definition of ..... ta ond 247
description of..... os ative Ba cad rat os 308
Montmorenci Falls, E. Emmons on....... 114
J.J, Bigsby OD... ..2p-ecssnu0d foe aint 116
Mosquito Range, Colorado, section. .....-. * 352
Moss Agate Springs, Montana, section... 325

Mount Desert, Maine, C. H. Hitchcock on
BOQUE G6 oo cdlak kn 6.00 as Sea dete 68
N.S. Shaler on rocks of .............- 69
Mount Putnam, Idaho, section ........... 161, 322
Mount Stephen, British America, section. 164
SEOMHILS REO, 3i/\5 vin. ens s woheein eee te 170, 171
Murphy, North Carolina, rocks of........ 138, 139

Murray, Alexander, on rocks of New-
POONA G oe dak nnenin ss -inaghan cae 52
on rocks of Canada.........-...+.-<- 208

N.

Nahant, Massachusetts, A. F. Foerste on
ROCKS Ofs oi omc dutam «neni oe eee 78
A.C. Lane onrocks at, cited.......... 78
J. H. Sears on fossils from............ 78
A. F, Foerste on fossils from. ........ ° 90

can S *
4
o¢
2
©;

eel
+.

442 ‘TDR, ESAS WRU Rbvi bed Satna) |)
: 3 . . 7 thes ae ey ¥ sn —?
Page. Page.
Nahant, Massachusetts—Continued. New York, J. D. Dana on quartzites: of alae
stratigraphical position of limestone. 271 COSEAIR, « cpninn's otaos align debe ata tities 109 <4 2
W. O. Crosby on rocks of........----- 271 Cambrian sediments of ............ an ,
Nason, F. L., on Cambrian of New Jersey °123, 287 problems for investigation in ........ 381 ve
Miepigen Sefeeiesnaekits pn: se~~-~ 0542000 339 | Nicholson, H. A., on life zones ..........> 424-425 a
Nevada, G. K. Gilbert on rocks of.-.-...... 156 | Niobrara River, Wyoming, section. ..-... 350 ty
E. E. Howell, on rocks in...... bw AB 4 156 | Nisconlith series,G.M. Dawson on....... 165 H
Arnold Hague on rocks of ...-.-.-- 158, 159,160 | Nomenclature of formations ............-. 18
Newberry, J.S.,on age of Lake Superior Nomenclature, geologic, general consider- F
¥ EE FE PO 194 Stlons O00... 52 - sou cas dese eee 236-237 |
on rocks of Texas .........-....-...- 218 | Nomenclature and classifications, prob et
on rocks of Arizona ............-.---- 219, 220 lenna OF... 225-5. -5-..«2. ae 388-390 doe
New Brunswick, A. Gesner on rocks of... 59 | North AmericanCambrian compared with a
W. B. Rogers on rocks of............- 60 Harepee® ».5...<22-J>«nboue wank tiles 372-377 *
J. W. Dawson on rocks of......-..... 60 | North American and European forma- : hs
J. Robb on rocks of............-....-- 60 tions, compared ............-----. 414-421 2
J.F. W. Johnston on rocks of...--..- 60 | North Attleborough, Massachusetts, N. ::
G. F. Matthew, classification of rocks S. Shaler on rocks of............-- 17 .

G8... cane echcan skedt eee a ee funstia Troi. -..c2 oS) Saaan ee 39 =
L. W. Bailey on rocks of...........-.- 61,64 | North Carolina, Cambrian rocks of -. .138-139, 299 i
G. F. Matthew, on rocks of........-.- 62, 64 problems for investigation in .....--. 383
Cambrian rocks of.................--- 273,274 | Northern Appalachian district, definition ;
problems for investigation in..-....-... 381 OD). Sep a'sGaswen tnah er nbe tyecneeieen 91, 275

New Brunswick and Cape Breton, Cam- paleontology OF waco ost oh teckeenee 148-154

brian rocks of............-.- 59-67, 262, 267 distribution of strata of...........- nett
Pedals freon ..3. 25. Ssdnds -eueaeen sees» 80-88 Cambrian rocks of............. 91-122, 275-287
CoP Bart C0 onis cae pce sundae tibeenices 80 | Northern Appalachian Province, sedimen-

Billings Of... .teedeoc-n os ee ere 80 tation in. .. 32 ....kesed eee 284 :
C. FP. Matthews, Oss. 00. cscccns ccccse 81-88 sediments of ............---..- 308-309, 312, 313
ah Walests. 60. <c case cusigennees fn 2s 81 TOBA OF a obs cacaedinn en epaerae eae 371
New England, C. H. Hitchcock on classifi- Norwood, J.C.,on Lake Superior rocks
cation of rocks of..........-.<..-- 72 CU 0 ei oe ee fens Se ae 175, 194
Newfoundland, historical review of work Nova Scotia, Cambrian rocks of......... 56-59, 262 .

ER pees Ra aes cei! At ale | oy: “- -- 50-55 A. Gesner on rocks of......-......... : 56
J.B. Jukes on rocks of..............- 50,51 problems for investigation in -....... 380
J. W. Salter on Paradoxides from.... 50,78 | Nova Scotia gold field, J. Campbell on. ... ~57
C. T. Jackson on rocks of...... ...-.- 50 A. RB. C. Selwyn: emo. c...k ne eee mn’: )

H. W. Bayfield on rocks of......-...-.- 50 HY, find 8.52 idee ns 58
succession of rocks in............---- 51 | Nova Scotia metamorphic slate, J. W. ;
W.E. Logan on rocks of....-......--- eR Win Dewan G01. 5,.273)., caees £23% o¢ 57 |
Alexander Murray on rocks of.....-. 52 | Nova Scotia gneissoid series, H. Y. Hind NOR MS
primordial formations in-..........-.- 53 GR. os dcucinanstsapany eee een > 58
J. Howley on rocks Of. <<... sececa=s5 53

A. Hyatt on fauna of.......-.-..---.- 54 O.

J. Milne on rooks of. ..........2...ce20 54 |

C.D. Walcott on rocks of.........-. 54, 55,113 | Obolella pretiosa, range of............... . 286
G. F. Matthew on rocks of.-.........-- 55 | Ocoee, definition of...........--.---+---..- 252
Rvbtler eten |. 2,0); 3. a eee ceen 78-80 | Ocoee conglomerate, description of. ...-- " 143
pre-Olenellus beds of........-....-...- 261 Bailey Willis of... ...05. dae. scuee ese 299-300
northwestern, Cambrian rocks of-..-.. 253-256 | Ocoee River, rocks of ..... chide thy Sages 141
southwestern, Cambrian rocks of-.-... 258-256 | Olenelins, range Of -. .. 2.2.5 c5cccneneamss 319, 370
eastern and southeastern, Cambrian Olenellus fauna, range of . . . .280, 281, 310, 362, 386—

POCA OL ct i205 Gat Aweemwes eee 257-262 387, 389 —
Cambrian sediments of............... 309 | Olenellus gilberti, remarks on............ 319, 329
problems for investigation in ........ 380 | Ophir City, Utah, section........-.. 156, 158, 319-326

New Hampshire, Cambrian rocks of .70-72, 267,268 | Ordway, A., on fossils from Braintree,
C. D. Jackson on rocks of............- 70 Massachusetts. .......-....-.-.s- 89
C. H. Hitchcock, classification of rocks Owen, D. D., on rocks of ‘Wiskoucie --171-172, 173-__
ES iindsn ons eeGibie ted aoaden +0%% 70-71 175
New Jersey, Cambrian rocks of....... 122-123, 287 on rocks of Minnesota ........-..-.-- 181
Seals CF 5... pdquesan dweuen eae capt 154 on rocks of Iowa.......--. waa seek an 1&7
problems for investigation in ......-.. 382 on Lake Superior sandstone ....---.-. 190-191
Newport, Rhode Island, W. B. Rogers on on fossils of Upper Mississipi valley . 221-222,
SACKS Obs Finns ck. Fo ous ee 76 223 —
Newton, Henry, on rocks of Black Hills.-. 216 | Owen, Richard, tabulation of rocks ...... 206

my i, * “he a i me 2 - 7° a dy L palin |
1 tks erm f ? ¥
ouees < - ‘INDEX. 443
Ss - Page. ; Page.
Owen, R., on fossil footprints of Canada.. 230 | Potsdd4m—Continued.
Ozark uplift, Missouri.................... 199, 201 rrr epee 341-342
> 4 g New York, section ...............-... 342
¥. formations correlated with........... 360
lati ith N Y
Paint Rock, North Carolina, rocks at..... 138 ny Faw! Sto ow toe 408-409
Paleontology of Newfoundland . 78-80 po es oe eos =s0" 8 eae
Paleontol f the North ee. oh- Potsdamic, proposed by C. H. Hitchcock. . 252
ania : ehh % “9: anlar ee 148-154 | PWell, J. W., on rocks of Arizona. ...... 220-221
ae Pi eee ak pose. Primal, definitionof........... dy ds = Sg ee
wen : opy © See ee n Primal series, H. D. Rogers on..........- 125, 126
ets --*----------- ve eographical distribution 126
Paleontology of Upper Mississippi area.. 221-228 ace BBO Ee Wie eee
{ ORGUG'OG 65565 ua eee eed ine sa nee 126
Paleontology of the Adirondack sub-prov- ival f
en = _. 999-939 OQmlyalonisé Of. 1055 ila capabs sande 126
= ia 7 a ear rae a sedimentation of.........2.Jccecssas- 126
Paleontology of ‘the Rocky Mountain h ,
shown on sections...........--.-.---- 126-127
, sub-province A PE CARESS 233-234 i Petes an 128
__ _ Paleontology of Arizona.........-------- 235 P. Deenapity iit hot ieeee Lae 129
cy A Peale, A. C., on Gallatin River, Montana. 162-163 alt al Ji. Sl) pee ee
Dak + LOGOY OW). 6 25> ce dew ase eeed 129-130
on rocks of Idaho............... bees 161
R Of Maryland 3 2 6 as -senstsincgs acon 133, 289-290
on rocks of Colorado .....-........--- 209-210 oo 4g
? W. B. Rogers on Virginia ...........- 133-134
Pennsylvania, Cambrian rocks of.124-132, 288-289 M AR oe
Pennsylvania, problems for investigation | Serpent ta race: Ss _
A an ; 389-383 W.-M. Fontaine on Virginia.......... 135-137
hen «. 7... ff of Petinsylvawte vi s32066.00nto ee 289
Percival, J. G., on Wisconsin, cited. -..--- 175 al Vives 3254.2... <5 es 290-291
Perkins, G. H.,on Winooski marble...... 110 | Primal slates and Potsdam sandstone, H.
Perry, J. B., classification ofrocks........ 105 BD. Lawisew ..::....2. 131
on red sandrock . spichge bie Spe aes ome 105 | Prime, F., on fossils of Pennsyivania.... 128
Pioche, Nevada, section... es ae ghee aha _ on Potsdam of Pennsylvania. ....- 128, 131, 288
Pogonip ridge, Nevada, section........-.. 158 on primal slates of Pennsylvania. -..- 128
Point Levis fossils, E. Billings on....-.--. 146-117 Primordial, in Newfoundland......-.-..--. 53
Portland, Maine, C. H. Hitchcock on of Virgiiie <ioo 0 S25 noon ecesiees 135, 294-297
rocks about .....-.--.---.-------- 68 detiniilan. Of cede 2. adus »cdpcebeetge 243
Portneuf range, Idaho, section........... 321-322 fant ot Novada’......2.< .2.-.20. et 155
Potsdam, C. H. Hitchcock on Vermont... 105 | Prospect Mountain, Nevada, section..... 158, 252
of Adirondacks, New York.......... 113-114 | prospect, definition of .........-..---.-+- 159
: G. H. Cook on New Jersey...--..-... 122-123 | Prospect Mountain series, fossils of. ... - B15
4 sc ¥xpo on Pennsylvania ....-.....- 128 dedetiption GF iccawavn ss. i cpeodagdps 313, 314
ae d'Tnvilliers on Pennsylvania......... 130 | Protozoic, proposed by A. Sedgwick -.-... 238
i T.S. Hunt on Pennsylvania. ......... 132 | Prout, H. A.,on fossils from Potsdam, of -
: T. D. Rand on Pennsylvania ........- 132 ee ee fe mie ee, hg de 292
W. B. Rogers on Virginia ...-....... . 134 | Ptychaspis piochensis, range of .......-.. 170
J. M. Safford on Tennessee..........- 142-143 :
E. A. Smith on Alabama .......-....-. 147, 306 Q
I. A. Lapham on Wisconsin.......... 172
J. Hall on Wisconsin ........... s-.-- 175-176 | Quandary creek, Colorado, fossils of...... 352
Wisconsin, compared with eastern Quebec, J.J. Bigsby on rocks near....... 114
8 aon a apg en 176-177 Cambrian rocks near..............-.- 285, 287
' description of Minnesota, 181, 182, 183, 185, 187 Cambrian sediments of.............-. 309-310
fossils of Minnesota ............-..--. 182, 183 R. W. Ells on the rocks of Province of. 120-121
E. Emmons on New York, 202-203, 204, 205, 206 | Quebec province,C. D. Walcott on rocks
L. Vanuxem on New York......-..-... 204 a ee Ey ee elo 121
EE SS Se ee a 204,205 | Quebec gold fields, A. R.C. Selwyn on..-.. 58
ee 205 | Quebec group, W. E. Logan on........... 116, 117
MEGS 56 5's dn weCudegenicad- ae 205-206 ‘A. B.C. Bela gm Gt .2n<2ciwieins Seaaden 119
Semen On BOW VOTkK....cccsaccsence- 205 foontin of, in: Wtah. os. s2., camehetebos 157-158.
T.S. Hunt on New York............. 206 rocks of, in Wyoming....-........-212, 213, 351
J.J. Bigsby on New York............ 206
C.D. Walcott on ...................2- 207 R.
IR nd ale icldcaseen pecnane 207
Beecher and Hall on................- 207 | Rand, T. D.,on Potsdam of Pennsylvania 132
ea maine tine Sb iat wins © 211-212 | Red sandrock, description of ........-.... 96-98, 250
Ee 217, 218, 219 FE Marcoa 6m. ..cn0-dencoueees aedte 103
I Ms ens anan sor cnvons cams 244 J. Wi EP Ocry 00 -x.-o<ncs pen eeeeienaeee 105
of Newfoundland................... " 254 C. EL. Hitchoogk G0 . .: 5<sscensaeeheue 106
Ee E SE its an nclasinwneeuss uae 332-334 J. Di, Dake C8 oa ccckecntnedvnckacne Je 107

Saint Croix district, Wisconsin, section .. 333-334
Saint John, New Brunswick, work of J.
W. Dawson on rocks at ......-.-- 61

RT f See at Atte eae eet eM er a rd
Stats $ beri ks en thrice were eed et earns my Me
F ( we wy J Pears. { me ye
' | ; ‘ p 4 iS : ; ie ‘ uy . ™ A si }
444 | INDEX. — i 8
Page. Pa
Red sandrock—Continued. Saint John, New Brunswick—Continned. La
Glatribution 66s hc veils os 277 G. F. Matthew on rocks of.......-.... 64-65
GHOLACtOR Giip as wameneubstsec ess --acce 277 G. F. Matthew on pre-Paradoxides
Richardson, J.,on rocks of the St. Law- g0n6 Gt... 520k eee ee ee ,...65, 67, 86
pe ROMO MEME Bo col clee cs caccsen's 118 pre- Paradoxides, beds of........._..- 264-265
Petey, We fiitte Ob tees ne Sok wc. ewsctaee 246 C.D. Walcott, on fossils from........- 81
Robb, J., on rocks of New Brunswick.... 60 A. Hyatt, on fossils from.......--....- 82
Rockfish Gap, Virginia, section - ..291, 292-293, 294 | Saint John group, C. F. Hartt on........- 62
Rocky Mountain province, problems for Matthew and Bailey on .........-..-. 62
investigation in.......-.-...--.-. 384-385 CoD. Walcott on: 0605s scab pds ane 65
Pemmntion of. 56. oe 155, 313 definition of.......-..-..-+--.-+++ ody pee
Cambrian rocks of ............ 155-165, 313-329 Geseriptiim. Offside wc. 6000s nee aad 263-264
paleontology of ..... Silt hea pete ee 165-171 Siviclons'6f 550 205.c. 20 1 tens Stine 266
Spaineniation ef 3..2...\..2- oosouceeee 328-329 | Saint John, O.,on rocks of Idaho ........ 161
Rocky Mountain sub-province, paleontol- on rocks of Wyoming. ....-- -. -213, 214, 350-351
DIP WE < cnt Uns Gadi n Pome . 233-234 | Saint John’s slate, description of........- 50, 51
7 a Re ERM 5 347 J. F. Whitesvos. On... <0 <genqacascses «5d
Cambrian rocks of .....-..00.2s--.c- 347-354 definition Of... .v..6.i vane 248
Roemer, F., on rocks of Texas.......--.-- 216,217 | Saint Lawrence River, W. E. Logan, rocks
fossils froin TRexkas ..25. 0. cee eee 234 ONS wistetn cine darn rete sina alee 115, 118-119
Rogers, H. D., classification of ..........-- 94-95 J.J. Bigsby on rocks of ...... -...--- 116
on rocks of New Jersey.....-.---...- 122 J. Richardson on rocks of ......---.-- 118
correlation of sandstone No.I........ 124 | Saint Louis, Missouri, section in well-.... 200, 340 —
on rocks of Pennsylvania..........-. 124-127 | Saint Peter’s sandstone and Chazy lime- ;
description of Primal series ...... - 125-126, 289 stone compared .....--...---.-- -- 176-177
on South mountain rocks. ............ 128 | Salem Village, New York, section........ 282-283
on Lake Superior sandstone.......--. 190 | Salt Range, India, section ................ 378
principles of correlation.......-..-.-. 417-418 | Salter, J.W.,on Paradoxides from New-
Rogers, H. D. and W. B., definition of fonndland:: v.26 vesbane =e ewe dooms 50
Péhnal »."..3. Nea 251 . fossils of Georgia..........-...-..--- 155
on correlation of rocks...-.........--. 403-404 on Tremadoc slates. ..........--.-..-- 241
Rogers, W. B., on rocks of New Bruns Salter and Aveline on Caradoc......--..- 239
WIG... oun ees ee 60,61 | Saratoga, New York, section......-..-... 346
on rocks at Braintree, Massachusetts. _73, 74 | Saratoga section compared with other sec- ;
on fossils from Fall River, Massachu- TOME fae ws case wn cgte wn age eae 346
eT Ae pe OE ar LaF) Jag” ede 75 | Saratoga County, New York, J. H. Steele
on rocks at Newport, Rhode Island... 16 on F6cKs Of, .o.05. 00 ns eee ree 201-202
on fossils from eastern Massachusetts. gg | Sardinia, Cambrian rocks of island of.... 375
on Primal series of Virginia. . .133-134, 290-291 | Scandinavia, Cambrian rocks of. -......-. 375
sections in Virginia.............-.... 136 | Schell Greek Mountain, Nevada, fossils of - 158
Rogers, W. B. and H. D., on lithologic char- Schoolcraft, H. R., on age of Lake Superior
acter in correlation..............- 428 BANAStONE « . 3. -'-- i cay eae ahaa 194
Rome sandstone, definition of ............ 047 | Scolithus linearis .131, 132, 137, 147, 172, 306, 404, 407
Rowinger, C., on Lake Superior sandstone 196, 337 | Scotland, Cambrian rocks of..-...-..---.- 376
Rosenfield station, Canada, section...... 334 | Sears, J. H., on fossils from Nahant, Mass. 78
Secret Cafion shale, definition of.......--. 246
S. description Of «6. onc} se ee betes ener 315
Safford, J. M., classification of rocks in TGUEO OF 35 ie 2 on to fn eee tee ae Pa 315
EIOOHOG. oes da Skano wate pee 141-142, 144 | Sedgwick, A., on Upper Cambrian . - - -237-238, 239
metamorphic rocks of eastern Tennes- on Middle Cambrian ~ . ois cdteas coon 238, 239
BEN ORES = otic ccs Ee Een rae 142 on Lower Cambrian .......<....ase0= 238, 239
Potsdam group of Tennessee. ........ 142-143 | Selkirk, British Columbia, section.....--. 165
fossils of Tennessee..............-.-. 154 | Selwyn, A.B. C., gold field of Quebec and
definition of Chilhowee .............. 251 Nera Boos... 0. eee oe
definition of Ocoee.............-.--.- 252 on Cambrian group sc. acccssocdeusnse 119
on rocks of Tennessee. ..........----- 300-302 on the Quebec group..... eS Rae 119
on classification of rocks ............ 405 on Lake Superior sandstone........-- 197-198
Saint Albans, proposed by J. Marcou. ... 281 on volcanic portion of Cambrian.-.... 286-287 —
Saint Croix, N. H. Winchell on Minnesota. 182, 183, Shaler, N.S.,on rocks of Mount Desert,
186 MaINO ds once. wdacaes abe Jeenecene ~ 69
elinitied. Of... {05 oR Cia aee wn, 245 on rocks at Braintree, Massachusetts. ae
description of... cee ee. 330-334 on geology of Bristol County, Massa-

chiinett hy) 3.075 Seren ee aes 17, 271-272

Shaler and Foerste, on fossils of eastern
Massachusetts. .........cn00-0005

:
¥

. Otay Sma picid! 4 SR As 8 Gl See
ones 4 Bi oy leer eee I bie! Be Mia a

1 i Se SOE eee eee ee eee ee eee 141-142, 144

' INDEX
‘ 3 :
. ‘ Page. Page
| Shaler and Williams on rocks of Little Tennessee—Continued.
‘Falls, New York..........-. .--.. 207, 347 J. B. Elliott on rocks of -.......2...-. 144
Shumard, B. F., on W isconsin, cited....-- 185 Cambrian fauna of .....-..........-.-- 154-155
Deen ROOks Of TOX@S..-.........-...----- 217 Cambrian sediments of ......-......- 311
fossils from Wisconsin and Missouri. 223 problems for investigations in. ...... 383
fossils from TOXAS .......02+--------- 234-235 | Texas, F’. Roemer, on rocks of...--....-.- 216, 217
‘Signal Hill sandstone, description of... .. 50, 51, 52 Cambrian rocks of.-.-...----. 216-219, 354-356
Sillery series, position of.........-..----- 286 B. F. Shumard on rocks of.....-...... 217
Sioux quartzite, description of ........... 182, 185 S. B. Buckley on rocks of .........- we 218
ia in vp wna nsdn bec eneens 185 C.D. Walcott on rocks of .........-.. 218
Ee emp sie 184-185 T. B. Comstock on rocks of .......... 219
Smith, E. A., work of, in Alabama...-..-.. 146-148 W. P. Jenney on rocks of .....-..-..- 218
on metamorphic rocks of Alabama... 146-147 J.S. Newberry on rocks of ........-- 218
on classification of rocksof Alabama. 147 paloontology of «2 3 jad coos sa cseeabs 234-235
on Potsdam sandstone of Alabama... 147 Cambrian sections of, compared with
definition of Montevallo ......-...... 247 PURRTEL 2. 6. kv d alten es a ee 355
definition of Coosa .........--.------- 247 - division of rocks by T. B. Comstock. . 355-356
definition of Weisner .........-.-- map 251 problems for investigation in ........ 385
on rocks of Alabama. .....-.......---- 305-308 | Thompson, Z , on red sandrock.........-. 97
Smock, J. C., on the rocks of Dutchess Timpahute range, Nevada, section....---. 156
County, New York .-...-.--..--..--- 111 | Tonto group, description of...........--- 220, 221
Snowden slate quarries, Virginia, section. - 297 | Tonto sandstone, definition of .........-. 245
South America, Cambrian rocks of..-.... - 379 description Ofc 5 oc .0 6s onde cd amas 357
South Mountain, Pennsylvania, H. D. Topsail Head, Newfoundland, section. - - - 52
Rogers on sandstone of ....... 124, 125, 128 TORSBIS GL. Jens. Paco tk ns Cee cee ee 55, 260
Mek. OSIOY OR... so. cnec-n- eee neee--- 127 | Toughkenamon division. .-.--.......---. 130
P. Frazeron....... A ees ahs at 128 | Toumey, M., on rocks of Alabama. .....-. 146
Southern Appalachian district, definition Tremadoc slates .......--...---- heer 241-242, 374
aes Pes aint 6 mien aon > mes 122, 287 | Trenton limestone, distribution of-...... 405-406
Cambrian rocks of ......-.----- 122-145, 287-308 | Trinity Bay, Newfoundland, section -.... «BB
paleontology of ........-...-..-..---- 154-155 | Troost, Gerard, classification of rocks. ... 139
Southwestern sub-province, definition of. 216, 354 on rocks of Tennessee. .......-.--..- 139-141
Cambrian rocks of ..-.......--. 216-221, 354-357 on Cambrian systemof Tennessee. 140-141, 240
PIII, 85 oso ost n ese cucuesnacees 357-358 | Trout Creek, Colorado, section....-...- 209-210, 353
‘Spring Creek, Dakota, section.......-.-.... 348 | Troy, N. Y.,S. W. Ford on rocks at ...... 106
Stevenson, J.J., on rocks of Virginia. .137, 298-299 J. Hall on fossils from ............--- 99
Steele, J. A., on rocks of Saratoga County, Tyson, P., on rocks of Maryland......... 289-290
: TR OR d ab awia owas aeonen ces 201-202
, on fossils of Adirondacks ......-.--.. 229 U. :
Strait GERalieiale,Newioundland, rocks | poe Cauubrian in Atlantic Const, prov:
eee IDOR ad | tna am ot ase ka teomerts aac 274
pereng, Moves, oy rocks of i, leone en Upper Mississippi area, definition of --.. 171
Sutton Mountain anticlinal, Canada...... 286 Paderinniepaks of... coo ee Sk 171-199
_ Swallow, G.C., on rocks of Missouri ..-... 199. 200 paleontology of 2.2.0... pe: Gy 221-228
Swanton, Vermont, section ..........- 103, 279-280 u Mississit i Valley.Cambrian ae
Sweet, E. T., on rocks of Wiscensin, cited 178 cece PP ys
: Ob cciccvik decree dente toe 330-334
on Lake Superior sandstone. ...-.. 196, 197, 337 problems for investigation in ........ 385
T Upham, Warren on rocks of Minnesota,
‘ 7 Olid ok Sawnkeaehsihath cee as 186
Taconian, definition of ...... ...........- 243 | Utah, F. H. Bradley on rocks of. ......... 156, 157
Taconian system, pre-Cambrian.......... 132 Clarence King on rocks of........... 157
Taconic slate, A. Fitch on................ 98-99 S. F. Emmons on rocks of ..........-- (157-158
SPM MGS Oh. .o--20c-n~ scwkce sane 99 Cambrian rocks of ote ce meen e ene eeee 319-320
Taconic group in Minnesota ........---.. 185 | Utah and Nevada, Cambrian rocks of. . ..155-160,
Taconic system, E. Emmons on.....-... . 98 312-320
J. Marcon on Lake Champlain ....... 108 fossils from - ninigure Bag 8 RA Oe ae 169, 170
DS Sitroor ON...-.. +... TAT a ae 109-110 problems for investigation in ........ 584
J. Marcon classification of..........-. 112-113 Vv.
GeGnition of. ....-.....-...- aa tae Regs 242-243
Tennessee, G. Troost on rocks in .....-.-. 139-141 | Vanuxem, Lardner, on Potsdam sand-
Cambrian rocks of .........--- 139-144, 299-303 stone of New York.........-.---- 204, 205
work of J.P. Lesley on rocks of...... 141 | Vermont, C. B. Adams on quartz rock of - 95
_J.M. Safford’s classification of rocks ©. H. Hitchcock on quartz rook of. ... 96
Amos Eaton on rocks of......-.----.. 98

Vermont—Continued.
C. H. Hitchcock on fossils from ..-..- 99
oc. ki all on fone Ge ack oes... 2 5. o- cues 100, 102
formations of, C. H. Hitchcock on..-.. 104
T.S. Hunt on geology of .....---.---.- 104
C. H. Hitchcock on Potsdam in...,.. 105
A. Wing’s discoveries in.........--.- 107
Cambrian rocks Of. ..........ccccacns 107
J.E. Wolff on fossils of......-.......- 113
T.N. Dale on rocks of. ...........--.. 283
Cambrian sediments of...........-..- 310-311
problems for investigation in.....-... 381-382
Verneuil, Edward de, principles of corre-
RITEOWS Sone weiss s daswaes cade eameete 414-415
Virginia, Cambrian rocks of -..-.- 133-138, 290-299
B.S. Lyman on rocks of......-.-..--. 134
A. McCreath on rocks of ............. 135
J.L.and H. D. Campbell on rocks in-- 136
H. D. Campbell on rocks of..........- 137
J.J. Stevenson on rocks of.....-.. 137, 298-299
W.-M. Fontaine on rocks of ..-.... 291, 292-297
Cambrian sediments of .-..........-- 311
problems for investigation in ...... =e 383
ho
Waagen, W., on fauna of India..........-. 378
Wadsworth, M. E., on rocks of eastern
Massachusetts...........-......- 76, 77
Lake Superior sandstone ............ 197, 198
on Braintree quarry .........-....... 271
Walcott, C. D., on rocks of Newfound-
RD Pe Pe NC my 54-55, 113
an SE olin: peup-i5 se. Jceupe apes 65
classification of the Cambrian. .....66, 77, 113
on fossils from Braintree............. 89
. on the Cambrian of Georgia, Vermont 110
on the rocks of Washington County, .
Now Werke. Rl Ree. 112
on granular quartz........-.--....... 112
on rocks of Province of Quebec...... 121
correlation of rocks in Tennessee... 144
fossils from Georgia slates........... 151-152
fossils of Lower Cambrian .......... 153-154
fossils from Alabama .............--. 155
eripediie of Utalie. 2c cstv wae ects 158, 166
fossils of Nevada ................. 160, 167-170
on fossils from British Columbia .... 163-164
on Potsdam of New York....-....... 207
on rocks’ of Terma... :.ts6 aleve 218
on rocks of Arizona ...:.......2..... 223
fossils from Wisconsin and Minne-
MM oe a. i setiotwtetobasa bien Sa 228
on fossils from Saratoga County, New
MOTs. & Sore meee wacks de an 231-232, 232-233
fossils from Black Hills.............. 234
fossils from Texas. ccnncccscccccwece 235
principles of correlation ............. 413
Wales, Cambrian rocks of ............... 373-374
Wasatch Mountains, Utah, section....... 157
sedimentation of...............cecces 328
Washington, Iowa, section in well ......- 188
Washington County, New York, section
Bh eo iitattw dvucennds cq shea eel 281-283

Waterville, Maine, C. H. Hitcheock on

+

ea

.
*
‘ . un
an

in, 248
an a

" fossil Of, ....55:ud aus eben et mo
Waverly gold district, Nova Scotia, SY:
Hind enti .= 5.225 ae ee = BT
Weber Cafion, Utah, section ............. 158
Webster, J. W., on rocks of Boston and i
Vidiniby -2..<-s'0 2900 dneeee eee 72
Weisner quartzite, definition of........-. 251
Geséription of... < .55 304, hee- ne 308 ©
Weisner, Georgia, section................ 304-305
Western border or Rocky Mountain sub- _
province, definition of ........... 209
Cambrian rocks of ..........-... <.--- 209-216
Western sandstone, description of. . . .197, 335-336
definition of. on owdsse essen eee 252
White, C. A., fossils of Utah ............. 166 _—
classification of rocks of Iowa..-..... 187
on fossils of Arizona............-..... 220-221
White, George, on rocks of Georgia ...... 144-145
W hiteaves, J. F., on slates of St. John’s.. 54
Whitehall, New York, section. ........... 344-345
Whitfield, R. P., on fossils from Braintree, _
Massachusetts .............-.-..- 89
correlations af; . /.2,c5 dure dee eee 108-109
fossils of northern Vermont .....-... 151
on fossils from Black Hills......-. 216, 233-234
fossils of Wisconsin.............. 2... 226-227
Whitney, J. D., fossils from Nevada...... 155, 165
on Lake Superior sandstone ......... 194, 198
principles of correlation ............- 411.
Whitney and Wadsworth on copper-bear-
ing roeks, C100), . /.,pce<e-cs00eae 198-199
Whittlesey, C., on rocks of Wisconsin ... 172-173
on Lake Superior sandstone.......-.- (195
William’s Cajion, Colorado, section ...... . 352
Williams, H. §&., on life history in correla-
tion, cited REE ee aA ee Sle 426-
Willis, Bailey, on Ocoee of Tennessee. - - 289-300
Winchell, A., on rocks of Wisconsin.:.... 178
on Lake Superior sandstone. .-....... 194
fossils from Wisconsin......... ayes 225-226
Winchell, N. H., correlations of... .109, 184, 186, 187,

207, 409-410
on rocks of Minnesota..............-. 181, 187
section at Emmettsburg, Iowa....... 187
on rocks of Black Hills .............. 216
fossils from St. Croix sandstone ....-.. 228
definition of St. Croix ................ 245

on lithologic character in correlation. 428-429

Wind River range, Wyoming, rocks of --. 350
Wing, A., discoveries in Vermont.-...-... 107
Winooski marble, E. Billings on.......... 103-104
C.'H. Hitchoock on « 5. <-cstepe dhs tease 105
GH, Perkina O08. -. js5.-setaneee sees 110
Winwood, H. H., on fossils from Kicking
FEGER. FORE Lo ons = won og es PE 163
Wisconsin, Cambrian rocks of-..-.-..-......- 171-181
D. D. Owen on rocks of........ 171-172,.172-276- ©
I. A. Lapham on rocks of. .......-.-..- 172
Charles Whittlesey on rocks of..-...-. 172-173
J. Hall on rocks of. .......c0e=s--- 173, 175-178
geologic map of.-.-........ feo ali ir ea 178
work of R. D. Irving in............... 178
A. Winchell on rocks of.........----- 178

T. C. Chamberlin on rocks in......-..

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