- w w . . h . l i ' .
W.
i l l . . ...(_Wl.f...UIV/^«l.
OK.'^IQI
V O L . 70. PP. 871-747. 19 FIGS.
References died
Black, Robert, 1954, Permafrost: A review: Geol.
Soc. America Bull., v. 65, p. 839-856, Figs. 1-3
Bucher, Walter H., 1953, Fossils in metamorphic
rocks: A review: Geol. Soc. America Bull., v.
64, p. 275-300, Pis. 1-2
Cloos, Ernst, and others, 1953, Reviews of geological literature: an innovation: Geol. Soc.
America Bull., v; 64, p. 255-258
Ingerson, Earl, 1953, Nonradiogenic isotopes in
geology: A review: Geol. Soc. America Bull.,
v. 64, p. 301-374, Figs. 1-6
Pecora, W. T., 1956, Carbonatites: A review: (}«lj
Soc. America Bull., v. 67, p. 1537-15SS
Poldervaart, Arie, 1953, Metamorphism of bj
rocks: A review: Geol. Soc. America Bull^ |
64 p. 259-274
Sharp,' Robert P., 1954, Glacier flow: A rev
Geol. Soc. America Bull, v. 65, p. 821-838J
COMMITTEE ON REVIEW ARTICLES IN GEOLOGY
Francis Birch
P. E. Cloud, Jr., Chairman
S. S. Goldich
J. Hoover Mackin
cffA
AREA
US
Granite
1 n^ IJ
RESEABSH fe^&f IIUTI
EARTH SS§iiO£ lABJ
T71—MWICnil/H
JUNE 18S9
GRANITE EMTLACERIENT AVITH SPECIAL REFERENCE TO
NORTH AMERICA
ao IHIM
BY A. F . BDDDINGTON
ABSTRACT
Publications of the last 25 years that discuss the emplacement of granite plutons
are reviewed, with special reference to North America. The plutons are classiGed according to emplacement in the epizone, mesozone, or catazone of the earth's crust. It is
found that those emplaced in the epizone are almost wholly discordant; those in the
mesozone complex, in part discordant and in part concordant; and those of the catazone
predominantly concordant. Granite formed by granitization is considered to be minor or
local in plutons of the epizone, common but subordinate in those of the mesozone, arid
a major factor in plutons of the catazone. The authors of the papers reviewed in general,
however, infer that magma was either directly or indirectly the major factor in all the
zones. Contrary to some current theories, this review emphasizes the great number arid
great total volume of granitic plutons emplaced asfluidmagma in the epizone and their
community of origin with lavas of similar composition directly associated in time and
space. Magma is thus inferred to play the major role in Tertiary stocks and batholiths.
There appears to be no discontinuity between plutons of the epizone and those of the
mesozone, and a major role for magma is indicated for the latter also. The evidence is not
clear as to whether plutons of the mesozone are continuous with those of the catazone,
have roots in the catazone, or are pinched off from it. Batholiths emplaced in the mesozone
are dominant in most basement complexes of Precambrian to Early Cretaceous ages.
SOMMAIRE
Les publications des 25 dcmifcres anndes qui traitent de I'emplacement de plutons de
granit sont pass^es en revue, en se rdfdrant sp&ialement 6. I'Amdrique du Nord. Les
plutons sont classes en fonction de leur emplacement dans I'epizone, la mesozone, ou la
catazone de la croQte terrestre. On a ddcouvert que ceux places dans I'epizone sont presquecomplfetementdiscordants;ceuxdansla mesozone complex, en partie discordants et en
partie concordants, et ceux situ& dans la catazone concordants de fajon pr6dominante.
Le granit forme par le granitisation est considdrd comme peu important ou ^pars dans les
plutons de I'epizone, courant mais secondaire dans ceux de la mesozone, et d'importance
majeure dans les plutons de la catazone. La plupart des auteurs de ces publications passdes
en revue ddduisent cependant que le magma ^tait, directement ou indirectement, le
facteur le plus important dans toutes les zones. Contrairement 6 certaines thdories courantes, cette dtude met en Evidence le grand nombre et le grand volume total de plutons
granitique emplace sous forme de magma fluide dans I'epizone; aussi leur origine communal h celle des laves de composition similaire associ^ directement ^ elles dansle temps
et dans I'espace. On en d^duit done que le magma joue le r61e de premier plan dans les
batholithes et les stocks Tertiairies. II ne parait pas y avoir de discontinuity entre les
plutons de I'epizone et ceux'de la mesozone, et, par consequent, on indique que le magma
joue dgalement un rdle important dans le mesozone. II n'est pas clairement Evident que
les plutons de la mesozone forment une suit ininterrompue avec ceux de la catazone,
qu'ils aient des racines dans la catazone, ou bien qu'ils se disjoindre. Les batholithes situfe
dans la mesozone dominent dans la plupart des complexes profonds de I'epoque Prdcambrienne jusqu' i I'epoque Crdtacee infdrieure.
ZuSAMMENFASStJNG
Es werden Veroffentlichungen der letzten 25 Jahre besprochen, welche die Position
von Granit-Plutonen, besonders solcher von Nord-Amerika, behandeln. Die Plutone
werden entsprechend ihrer Lagerung in der Epizone, Mesozone oder Katazone der
Erdkruste Klassifiziert. Es zeigt sich, daC die Lagerung in der Epizone nahczu vollig diskordant ist, diejenige in der Mesozone dagegen komplex, teilweise diskordant, teilweise
671
672
CONTENTS
A. F . BUDDINGTON—GRANITE EMPLACEMENT
Page
Mt. Monadnock, Vermont
.'.. 685
Ahvenisto, Finland
685
Other discordant granitic plutons of
epizone
685
Introduction
685
Stocks and volcanic rocks of western
Cascade Mountains, Oregon
686
Snoqualmie batholith, VVashington
686
Batholith, Casto quadrangle, Idaho
686
Boulder-San Juan discordant belt of plutons, Colorado
687
Stocks of Concepcion del Oro, Mexico
689
Boulder batholith, Montana
690
Seagull batholith, Yukon Territory
690
Precambrian plutons of epizone
690
General statement
'.
690
Granophyre
;
690
Ring-dike complexes
692
Aureoles of pseudo-igneous emplacement in
epizone
692
Description
;
692
Bingham, Utah, stock. . :
692
3AJIEVKB. rPAHHTA B CEBEPHOtt AMEPUKE
Cassia batholith, Idaho
692
La Plata stocks, Colorado
692
A. <D. ByanaHTTOH
Supplementary descriptions of plutons emplaced in the epizone
692
A6cTpaKT
New Cornelia quartz monzonite stock,
Arizona
692
IleHaTHhie Tpyflti nocjieAHiix nex, oniicuBaiomiie noJioKeniie rpannTHMX
Hanover stock, New Mexico
693
nnyToHOB, oco6eHHo Tpy«H iisAaKHbie B CeBepiiott AMepviiw flBjimoTcn
Marysville stock, Montana
693
npcRMeToM HacToHmoro o63opa. IIjiyTOHu KJiaccn$imupoBaHW corjiacHo iix
Organ Mountain batholith. New MexnojioxcHiiio B aniiBone, MecoaoHe IIJIII KaTaaoiie seMHofl Kopti. Bujio naftfleHO
ico
693
•iTo njiyTOHhi iiaxoAnniiiecH B aiinaoHe noirn nojiHooTbio iiccoBMecTiiMu; reme
Paleozoic leucogranite and granite porphyry batholiths, Newfoundland
693
B MeCOaOHHOM C O e a H H e H n i l M a C T U O H e O O B M e c T H M W II MaCTblO COBMeCTHMW
Plutons of transitional(?) epizone-mesoTorAa KaK TO B KaTasone rnaBHMM o6pa30M coBMecTiiMU. rpaHriT
zone
694
o6pa30BaMHbitt nyreii rpaHiiTii3annn paaoMaTpiiBacTcn KaK BTopocTeneKHuft
Introduction
694
iiJiH MecTHHtt (taKTop B HJiyTOHax aniiaoHa, o6biMHbitt HO BTopocTenenHtift B
Southern California batholith
694
njiyTOHax MecosoHa, ii nan rjiaSHHll ^auTop B nnyToiiax KaTasona. B o6DaeM
Batholith of southwestern Nova Scotia
695
aBTOpM cTaxeft HacTonuiero oSaopa onHaKO noiiycKnioT «ITO MarMa
Plutons of mesozone
695
iienocpeflCTBeHHO iinn nocpenoTBeHHO nBJiHeTca rjiaBiiuM ^[)aKTopoM BO BCCX
Introduction
695
soHax.
B
npoTiiBonoJiowHocTb
iieKOTopbiM
coBpeMeHHWM TeopnHM
Characteristics
695
Mesozoic plutons with both discordant
paccMoTpeHHMM B iiacTonmeM o63ope non'repKiisaeTcH 6ojibnioe KOJIH'ICOTBO
and concordant relations to country
II Gonbuioft o6'beM.rpaHKTHiJx nnyTOKoe BHenpeimux B BIIAC WHRKoft MarMu
rock
697
B 3nM30He II HX cpeBCTBo no npoiicxoHweHino c jiasaMii nono6H0ro we cocTaBa
White Creek batholith, British ColumH e n O C p C f l C T B C H H O C B n S a H H b l M H n o B p e M C H H II n p O C T p a H C T B y .
IIOBHflHMOMy
bia
697
ne oymecTByeT HenpepbiBnoll CBHSII MSMcny njiyxoHaMn aniisoiia H njiyroiiaMH
Sierra Nevada bathohth, California
699
Mecosona, iipn MBM maBHan poBb jx.nR MarMu yKasaiia TanHte nnn nocJiejiHero.
Coast Range batholith, Alaska-British
Eme He HCHO KBJIHIOTCH JIH nnyTOHw Mecosona HenpepwBHo CBnsauKbiMii c
Columbia
700
njiyroHaMH KaTaoona, HCXOJIHT JIH OHU 113 KaTasoHa HJIU oTntenJieHU ox Hero.
Mesozoic pseudo-igneous plutons or facies
of mesozone
701
BaTOJiHXbi, BiienpeHHbie B jiecosoHe iirpaiox rnaBHyio pojifa B GoJibineHcTBe
Swedes Flat pluton, California
701
ooHOBHwx Mace npeKaM6pHOHOBoft BHJioTb no paHHeft KpexacoBott anox.
Pellisier granite facies of Inyo batholith,
California
702
Chilliwack batholith, Washington
702
Mesozoic plutons with, protoclastic or lateCONTENTS
stage post-consolidation deformation... 702
Colville, Washington, and Cassiar, British
Columbia, batholiths
702
Pap
TEXT
Precambrian batholiths of mesozone
703
Late Tertiary cauldron subsidence and
Page
General statement
703
intrusion
681
Noranda-Senneterre belt, Quebec
703
Introduction and acknowledgments
674
Early Tertiary cauldron subsidence and
Plutons north of Great Slave Lake, NorthRead's "Granite Series"
675
plutons
681 i
west Territories
705
Zones of emplacement
676
Permian, Mississippian (?), and Devonian j Supplementary descriptions of plutons emPlutons of epizone
677
plutons associated with cauldron subplaced in mesozone
705
Introduction
677
sidence
682'
Introduction
705
Granite stocks and batholiths associated
Stocks primarily by cauldron subsidence,
Bald Rock batholith, California
705
_\vith ring dikes arid cauldron subbut accompanied by outward or upward
Snowbank stock. Minne.sot.i
'07
_^
680
pressure
^
6851.
konkordant, und diejenige in der Katazonevorwiegendkonkordant. Granite, welchedurch
Granitisation geformt wurden, miissen in den Plutonen der Epizone als verhaltnismaBig,
selten oder nurdrtlich angesehen werden, als regelmaBig, jedoch untergeordnet, in denen
der Mesozone, und als ein Hauptfaktor in den Plutonen der Katazone. Die Autoren der
besprochenen Verdftentlichungen kommen jedoch im allgemeinen zu der Uberzeugung,
dad das Magma, direkt oder indirekt, in alien zonen der Hauptfaktor war. Im Gegensatz zu einigen anderen umlaufenden Theorien betont diese Zusammenschau die groBe
Anzahl und den groCen Gesamtraum von Granitplutonen, welche als flussiges Magma in
die Epizone eingedrungen sind und unterstreicht ihren genieinschaftlichen Ursprung mit
Lavamassen ahnlicher Zusammensetzung, mit denen sie zeitlich und r&umlich in direkter
Verbindung stehen. Das Magma spielt infolgedessen eine Hauptrolle in tertiaren GranitstBcken und Batholithen. Es scheint keine Unterbrechung zwischen den Plutonen der
Epizone und denen der Mesozone zu bestehen, und fUr die letztere scheint das Magma
ebenfalls eine wesentliche Rolle gespielt zu haben. Die Bcweise sind nicht klar, ob die
Plutone der Mesozone in diejcnigen der Katazone Obergehen, ob sie VVurzeln in der
Katazone haben oder ob sie von ihr abgeschnitten sind. Die in die Mesozone eingelagerten
Batholite sind in den raeisten Grundmassiven vom Prakambrium bis zur Unteren Kreide
vorherrschend.
t
m
673
Page
Plutons of transitional mesozone-catazone.... 708
General discussion
708
Plutons of Wolverine complex, British
Columbia
708
Plutons of Shuswap complex, British Columbia
708
Williamsburg granodiorite pluton, Massachusetts
708
Lithonia gneiss (and Stone Mountain granite
of mesozone), Georgia
710
Prospect porphyritic granite gneiss (and
Nonewaug granite lens of mesozone),
Connecticut
710
Precambrian phacoliths of Hanson Lake area,
Saskatchewan
710
Syntectonic Pinckneyville batholith, Alabama
712
Complex history of great batholiths, largely of
mesozone
712
Introduction
712
Coast Range batholith
712
Idaho batholith
:
713
Complex of plutons in Appalachian orogen,
northeast section
713
Plutons of the catazone
714
Introduction
714
Domes
'
715
Introduction
715
Igneous domes of magma emplacement... 715
Interlayered xenolithic domes
.'. 716
Tectonic domes of plastic crystalline
flowage
716
Tectonic domes of remobilization with introduction of
fluids
716
Phacoliths
717
Introduction
717
Phacoliths of the Grenville subprovince,
Canadian shield. .;
717
Phacoliths of the New York-New Jersey
Highlands
717
Wolf Mountain phacolith, Texas
721
Harpoliths
722
Replacement pseudo-phacoliths
722
Phacolithic and pseudo-phacolithic emplacement, Manawan Lake area, Saskatchewan
722
Subcylindrical plutons
722
Emplacement m the Grenville subprovince,
Canadian Shield
723
General statement
723
Plutons in the Grenville series of Quebec
724
Plutons of northwest Adirondack area.
New York
724
Plutons of Haliburton-Bancroft area,
Ontario
,
725
Batholithic development of pseudo-igneous
granite in catazone
725
Introduction
725
Goldfield-Martin Lake area, Saskatchewan
725"
Quad Creek area, Beartooth Mountains,
Montana
726
Complexity of Precambrian plutonic complexes
728
General
728
Grenville belt
728
Colorado Front Range
728
Mackenzie district. Northwest Terri-
674
INTRODUCTION AND ACKNOWLEDGMENTS
A. F. BUDDINGTON—GRANITE EMPLACEMENT
Page
General structural relationships
731
Predominance of mesozonal batholiths in
plutonic complexes
732
Criteria for large-scale granitization
732
Emplacement of plutons in epizone and mesozone
733
Emplacement of plutons in catazone
736
Origin of granitic magma
737
Problem of volcanic and plutonic associations
739
Conclusion
•. 740
References cited
741
ILLUSTRATIONS
Figure
Page
1. Schematic relationships of emplacement
zones
2. New Hampshire belt of plutons
3. Oslo region, Norway
4. Belt of Tertiary intrusive stocks emplaced
in volcanic rocks of western Cascade Mountains in Oregon and Washington
5. Boulder-San Juan belt of plutons discordant to regional structure, Colorado
6. Tertiary granodiorite stocks emplaced discordantly in epizone
7. Seagull discordant Upper Cretaceous (?)
677
682
684
687
688
689
INTRODUCTION AND ACKNOWLEDGMENTS
A wealth of detailed descriptions of the
internal structure and external relationships
of granitic plutons to country' rock has been
published since the reports (1931-1935) of
Professor Grout's "Committee on Batholith
Problems", the review by Daly (1933), and
the memoir of Balk (1937). Read has meanwhile (1949; 1951; 1955; 1957) developed a
philosophy of the origin and genetic relationships of granitic bodies under the phrase
"The Granite Series"- which is a major contribution. Read emphasizes that the mechanics
of emplacement of granitic masses must be
interpreted in the light of their regional setting.
The writer proposes to amplify this idea further,
largely in the sense of an essay review documented with specific examples, based preponderantly on the pertinent literature of the
past 25 years that describes the granitic plutons
of North America. The plutons of North America are emphasized because the author is
better able to evaluate the implications of
the literature on tliem; and because the phenomena of the plutons of North America and
their interpretations have led to an emphasis
on certain mechanics and conditions of em>-~»ment_that is different from that of much
Figure
Pw, fc potentiality of formation of granite -by
batholith, Yukon Territory, emplaced in a , jranitization as well as emplacement by plastic
syncline.
W , oystalline flow. A review of the literature, in
18. Great discordant Devonian (?) granite • „
,
,
... , •
., ,.
j
.. i,
696 i pneral, makes it obvious that we do not yet
9. batholith of south-west Nova Scotia
Representative complex Mesozoic batholith
v hve dependable criteria that are acceptable to
698' geologists as a whole to distinguish between
10, of mesozone
Early Precambrian bathoUths of meso- ^^^^^ products of the different mechanisms of
11. Precambrian batholiths emplaced in raeso- ' tmplacement. There would also probably be
zone
706^ Bttle dissent from the view that such geologic
12. Williamsburg granodiorite pluton of transi- . problems will not be solved by field geology
, , ''O"'"!' mraozone-catazone
'• • • .i,- '^ ""i ilone, but by retention of what seems good in
13. Small Paleozoic pluton of mesozone (Stone , j . . .
.,
^ ^ .i • i •
j
AMountain granite, Georgia)
7U' «W >deas with constant rethinkmg and co-ordi14. Geology of part of Haliburton-Bancroft
j nation of new hypotheses, of data from new
area, Canadian shield
7)8. experiments and new laboratory studies, and
15. Precambrian plutons of catazone, north,(^^^
f^ (g^,^
j
j ^ ^ ^ ^ ^^^ ^^^^
west Adirondack area. New York, outlier
. „„ , , . . , ^„ ?, °-'
of Canadian shield
^ m ^ ^ ^'^^ of '"sight' idea.
In the discussion to follow the dividing line
16. Compound granodiorite phacoliths (M.L.
between a stock and a batholith will be taken
and S.L.) of intrusive origin and pseudofjhacolith of granodioritic gneiss (recrystal- ^ 4s roughly 40 square miles as suggested by
lized and granitized meta-arkose iti silti), p Daly. Granite, except where indicated othercatazone
7231 ifise by tlie context, will include the family
17. Two areas of Precambrian batholiths
72??
18. Geology of a part of the Front Range, 'j of granitoids such as quartz diorite or tonalite
"^ ind trondhjemite, granodiorite, quartz monzoColorado
72?,.,
19, Schematic sketch showing possible strucnite or adamellite, and granite or leucogranite
tural relationships of plutons in epizone, , and alaskite. The term pluton will be used
mesozone and catazone
lij
here in a very general sense for any body of
intrusive igneous (or "pseudo-igneous" by
, ,,
„
,.
, ,
• metasomatism or recrystallization) rock of
of the current European literature and deserve ,
^^^ ^^
^.
^^ ^^^ j^^^^,;^j^
review and consideration. A few exampl^ d ; ,.;,! ^^^^.^^ ^^^
•
^ ^ ^ ^ ^ „ ^ h e term
plutons from outside North America wdl te ^ ,^^^ crystalline flow here means, flow of
cited to exemplify or accentuate certam Ideas :^^j^^.^j ^^^.^ ^^_^^.^^ ^ j ^ ^ ^ ^ ^^ p^^^^^i.
or phenomena.
ri„,H | " ^ t l y crystalline during thoroughgoing deThe writer is indebted to Preston E Cloud, j(^^„^^;^^ ^^^ .^^^^^^ the concept cf recrystalJr., H. H Hess, F F. Osborne, and Ane Pol-|,i^^j^^ tlirough partial melting or solution and
dervaart for friendly criticism and ^onstruc-lj^ .
. .
° .
tive suggestions. They should not, however, i j
be held responsible for shortcomings of the ,•
„
, „„
r.
»
review.
i
READ'S "GRANITE SERIES"
The problem of the origins of granite is,; Read's concept of the "Granite Series'
necessarily a factor in the consideration of, -^ay bggt tig presented by excerpts from his
the- mechanics of emplacement of plutons. writings.
Many geologists who believe that most granites j |
are formed by "granitization" or "transforma-^ „ (1^7, p. 79) "Intnisions have been clawed as
. ,, °
, , ., . ,,
1.1 - ' pre-tectonic, syntectonic or post-tectomc. I have
tion'^ repeatedly emphasize that the problem., mdeavored to codify these relationships in what I
must be solved by-geology and field evidence.^ call the Granite Series (Read, 1949), a series which
There is also the implicit inference that field,.: relates the nature and form of diiterent types of
geologists, with independent minds and famil- granitic bodies with their place in the fold-belt and
the time of their final solidification. The Granite
iar with the current ideas of granitization-; Series can be represented thus:
will find granitization the best hypothesis tO;
-TIMEexplain most or nearly all granites. Yet tie.
North American literature of the past 25 yeare N
-CRUSTAL LEVELemphasizes strongly the role of magma either; PAutochthonous Parautoch- Intrusive Plutons
directly or indirectly in the problem of em-^ rgranitization
tbonous
magmatic
placement of plutons. This despite the factl [granites, miggranites
granites
that the authors quoted, more than 100, are [jnatites and
field geologists who accept as valid concepts; KwptQ mrv».T-.l^| ^ « "
675
Deep in the fold-belt are formed, at an early stage
of orogenjf, great complexes of granitization granites associated with migmatites and widespread
regional metamorphic rocks. As the orogeny continues, a part of these autochthonous granites
becomes partly unstuck from its surroundings
and moves higher in the fold structure. This process continues with the movement of true intrusive
and magmatic portions late and high, and culminates in the emplacement of the granite plutons,
highest and latest, pushing their way as almost
solid bodies even into the post-orogenic sediments."
(1951, p. 21) "The resulting parautochthonous
granites show variable marginal relations, in some
places migmatitic, in others characterized by an
aureole of thermal type. This movement out of
the migmatitic-metamorphic setting may continue tiU the genetic ties are completely severed
and true intnisive granites emplace themselves in
higher levels of the crust maybe as magma but
more likely as migma. The final term of the granite
series is represented by the high-level pinions,
intrusive into non-plutonic regions late in the
history of the orogen concerned.... The plutons
are the domain of the Granite-fektonik of the Cloos
school and, as their emplacement produced considerable folding and distortion in the country rock
surrounding them, they came in as almost dead
bodies."
The writer believes that Read's discussion
needs some major revision.' Plutons with
"granite-tektonik" are not the final terms of
the granite series. On the contrary they belong
almost wholly to the mesozone where, as
multiple units, they may form huge batholithic complexes. The-final terms of the granite
series are the plutons of the epizone. Read
minimizes as "few", "puny", and "nearly
dead" the bodies emplaced in the upper levels
of the crust. This is wholly inconsistent with
the number, size, significance, and the evidence for mobility and fluidity of most plutons
emplaced in the epizone of.the crust in North
America. Knopf (1955, p. 697) estimates that
plutons of Tertiary age in North America and
Greenland (all emplaced in the epizone) have
a total area of 52,000 square miles.
Hans Cloos (1931) has presented a succinct
pertinent discussion of the possible structural
relationships of plutons at different depths. A
summary prepared by S. W.' Sundeen (1935,
p. 48-49) is quoted here
"In a single mass the inner tectonics differ at
different horizons. In the upper horizon there are
poor, elusive structures in irregular branching
stocks. In the moderate depths there are well- •
formed arches, schlieren domes, partitions or pendants of wall rock and cleavage with border deformation and mylonites; with or without a stretching
of the border spalls. In the deep zone there arc
arches of gneiss. The whole region is deformed and
moves with the marma ns an I'll-'Jofi-oJ .—••^ "
EMPLACEMENT
occurs not only before and during crystallization
but in part after. There is thus a lack of any small
dynamic border zone and a lack of fracture surfaces, border spalls and most other features of the
moderate zone. Cloos sketches a vertical section
of a composite of these three horizons, each mass
smaller and drained lip from the one below, and
with less foliation than the one below; but does not
deny that a single mass may grade downward
without much change in horizontal section into the
conditions of the deeper zone."
ZONES OF EMPLACEMENT
The granite emplacement series will be
discussed with emphasis on the internal and
external structure of the plutons within different temperature-depth or intensity zones of
the crust. Under the simplest hypothesis the
intensity of regional metamorphism may be
expected to increase somewhat uniformly with
depth and therefore afford an indicator of
..the depth. The site and period of granite
• emplacement, however, is not one of static
conditions but of dynamic changes' in the
"environment. This is especially true for the
•mesozone. The- intensity of regional metamorphism in belts away from the intrusives
may stiU be used, however, as a suggestive
clue to the depth zone, {See also Michot, 1957).
•. Inasmuch as we are particularly interested
in the physical conditions of the country rocks
a.t the time and in the region of emplacement,
the "upper and lower limits of each zone will
. have a considerable range of depth for different
regions and at different times in development.
The depths for plutons with similar characters
will depend on the temperature, pressure, rela, tive mobilities of the country rocks, and other
factors. The term zones as used here thus
refers actually in substantial part to iniemity
zones rather than strictly depth zones. At the
same level in the mesozone a. batholith may
be emplaced discordantly in only warm country
, rock during early stages and conformably in
hot rock during late stages, especially in the
' roof. A predominantly mesozonal pluton may.
have diaracters peculiar to the catazone in
,^ the roof portion; In some examples the estimation of the physical conditions may be
diflScult and little better than a guess. Nevertheless examples for which at least fair to
••' good data are available afford the basis for
a 'reasonably consistent picture and afford
some additional insight into the problems of
emplacement.
Michot (1956, p. 28) suggests that the epizone may be taken as extending from the sur-
ZONES OF EMPLACEMENT
677
The rocks of the granulite facies in the tons 2.5 billion years old may be of the type
face to a depth of 10 km. The mesozone and
Grenville
belt appear to represent those emplaced in the mesozone, as in the Keewatin
catazone will be successively below this.
formed at some of the deepest depths now belt of the Canadian Shield where erosion to
The development of the greenschist facies
of metamorphism in rocks could be considered • exposed in North America. They are estimated only moderate depths is indicated.
as a characteristic phenomenon of the meso12 Miles
10
zone. Fyfe, Turner, and Verhoogen (1958,
—' Deplh
_j
p. 218) estimate that it is unlikely to develop;
Epizone
below a temperature of about 300°C. and above
Mesozone
a depth of- about 10 km. Their curves (p.
Cotozone
182) for rise of temperature with depth suggest
that at a depth of about 10 km in a great
FiooHE 1.—SCHEMATIC RELATIONSHTPS OF EMPLACEMENT ZONES
thickness of sediments, after depression in the
earth's crust, the temperature might rise to
to have formed between 600" and 700''C. Fyfe,
PLUTONS OF EPIZONE
about 250°C., and where the temperature-' Turner, and Verhoogen (1958, p. 182) give a
had been increased by magmatic intrusion it
"Dr. Button's theory of granite. .'.at the
curve that indicates that a temperature range
might be as high as 450°C. A rise of temperaof 600°-700°C. could be reached at depths of same time that it conceives this stone to have
ture in the country rock above an intruding
9-13 miles where the gradient had been in- bten infusion, supposes il to have been, in that
magma is strongly implied by such data as
creased by magmatic intrusion. Rosenquist state injected amtnig the strata already consolithat given by James (1955). The magma may
(1952, p. 102) estimates the minimum depth dated." John Playfair, 1802..
thus be emplaced in rock of temperature higher
for the development of the granulite facies
that that otherwise appropriate for the general? in this temperature range as 9-10 miles.
InlroduiJiot%
region,
A depth
commonly- of 4 miles but withj"..
_
;,™, The predominance of mesozonal batholiths
I t is rare that estimates are given in the
occasional extension, perhaps, to 6 miles seems,-; ^ [^ basement complexes, however, indicates
literature of tlie depths at which the present
a reasonable estimate for the base of the epi- ^ ^ that only locally has erosion cut very deep,
zone.
_T
Possible depth relationships for the zones exposed parts of a pluton were intruded. Tertiary intrusions as now exposed may be expected
The depth of the base of the mesozone or.^ 'are shown in Figure I.
to have been emplaced within the epizone;
top of the catazone where the amphibolite.y
x^g^g jg j ^ the western Cordillera of North
the
time for subsequent erosion has been too
facies starts must likewise have a substantial | ^ America a rough correlation between the
range, perhaps from as shallow as 5 miles to^. .structural relationships and zones ot emplace- short to permit deep erosion. A review of the
as deep as 10 miles. Wegmann (1935) esti-j . ^ent of the plutons and their ages, especially literature shows that Tertiary intrusions have
mated the minimum depth of the "migmatitef :. (QJ ^^^^^ ^f L^te Jurassic and younger age. the following characters, and these will be
front" at 10 km. The temperature range for| i piutons of Tertiary age as now exposed were used as criteria in classifying intrusives in the
the mesozone may be estimated to vary froral ; exclusively emplaced in the epizone and may epizone of older ages.
about 250°-350° at the top to 500°C. at the base,
Tertiary stocks and batholiths are largely
be associated in space and general time with
Tuttle and Bowen (Adams, 1952, p. 38) I' volcanic rocks of equivalent composition and or wholly discordant to the country rock no
wrote that " I t is improbable that many granoften emplaced in them; those of the Late matter whether they occur in Precambrian
ites reaching the light of day have crystallizedt , Cretaceous are also emplaced in the epizone, schists and gneisses or in folded Paleozoic and
at depth greater than 9 miles". This seems
! but there are more large plutons; the great Mesozoic sediments, or, as is common, in
slightly low. The possibility that erosion has
i composite early Late Cretaceous (?) Southern gently dipping Tertiary volcanic rocks. Occaexposed levels at a maximum a few miles deeper
i California batholith has characters transitional sionally, as in the Gold Hill stock in Nevada
than this must be considered, but in general it is.i!
between those of the epizone and those of the (Nolan, 1935, p. 43-48), part of the walls are
probably of the right order of magnitude. Guten. mesozone, whereas the composite stocks and controlled by preintrusive faults. They may
berg (1957) cites figures of 35 km for the depth
i batholiths of the Late Jurassic and Early occur in limestones, a type of rock peculiarly
of the "granitic" crust beneatli the Alps and 1] Cretaceous were emplaced in the mesozone resistant to granitization, without any sugges25-30 km beneath the Sierra Nevada. If this II with earlier members of the largest batholiths tion of relics or inheritance by replacement. A
is assumed to indicate the depth of the down If emplaced in the catazone.
few gram'tic plutons may be effectively homogefolded sial, and if reasonable estimates are \l. Similarly, in the Appalachian orogen, the neous in composition, but most are of composite
made for the thickness of eroded material a
Dost-Pennsylvanian plutons were all emplaced character caused by a successive series of
figure of about 25 miles is arrived at as the, i in the epizone, whereas many earlier plutons magma emplacements of diverse composition.
normal maximum depth for sialic material
If of Devonian age were intruded in the mesozone, The diversity is commonly from syenite or
Assuming further that the minimum thickness: |i, transitional mesozone-catazone, or locally per- monzonite to granite, or from diorite through
of sialic basement complexes in the continental
quartz diorite, granodiorite, and quartz monzohaps the catazone.
shields is about 10-12 miles, the inference may^
Jl For rocks older than the Tertiary, however, nite to granite. Quartz diorite commonly
be drawn that present levels of erosion havej
I there is no necessary systematic relationship does not form- as large a part of plutons in
rarely exposed rocks that were ever at a depthj
between age of rocks and the deplh at which the epizone as it does in those of the mesozone.
greater than about 12-15 miles.
they were emplaced. Unmetamorphosed plu- Locally or in a few plutons the diversity may
678 *
A. F, BUDDINGTON—GRANITE EMPLACEMENT
be due in part to incorporation, more or less
in place, of country rock, especially in border
or roof zones, but this is usually relatively
unimportant. Roof pendants are common.
Many of the plutons are effectively 'homophanous without lineation or foliation. Some
have a primary linear structure, but welldeveloped planar foliation is uncommon and,
where it occurs, is usually restricted to local
border facies or is indistinct.
The orientation of lineation in tlie Jamestown, .Colorado, granodiorite stock has been
studied by Goddard (1935). He finds that the
stock IS elongated N.-S., that the lineation
along the western part plunges about 70°-80°
and in a re-entrant protrusion on the east has
a gentler plunge of about 35°-60°. Grout
(quoted in Calkins and Butler, 1943, p. 35-36)
studied the lineation of the Alta stock in Utah
and shows the linear structure plunging in
general 80° or steeper in the border zone and
:gently in the core. The lineation of both stocks
thus suggests steep upward flow in the border
zones. Grout and Balk (1934, p. 885)"find that
lineation in much of the Boulder batholith is
elusive, but most has a pitch of about 70°,
and a steep conformable upward rise is suggested. Both the Alta and Jamestown
stocks and also the Mount Princeton batholith
(Dings and Robinson, 1957, p. 30) have associated dikes with gently plunging lineation
suggesting subhorizontal flow. Other types of
orientation of flow lines such as arches of
flow lines and disconformable flow lines at
an angle to the walls have been referred to by
Balk (1937, p. 50-54, 60-63, 69-78)'. The arches
of flow lines may in some examples, at least,
be suggestive of an arched roof. •
Moehlman (1948, p. 118) and others have
referred to Tertiary plutons whose walls
converge downward.
Volcanic rocks are commonly associated in
dose genetic relationship with Tertiary plutons,
but they need not be with plutons of the deeper
part of the epizone. Characteristically, at
least, part of the volcanic rocks wUl have
compositions comparable to that of the facies
of the plutons tliemselves although the quantitative ratios may be different. Alper and
"^ Poldervaart (1957) have studied the Animas
stock in New Mexico and the volcanic rocks
it intrudes and have shown that not only is
the chemical and mineral composition similar
but the zircons of both the tuff and the pluton
• -'-'-Habits.
"'"•-"—'>f^tiie con tact-
PLUTONS OF EPIZONE
wm
metamorphic zones, may be relatively uo-i L The earlier members of a complex pluton, p. 69) to indicate that many plutons ot the
metamorphosed. If folded and regionally] Rin small or moderate volume, will show chill epizone have been emplaced as highly viscous
metamorphosed there may be independent! I tones against country rock. Dikes, apophyses, magma at relatively low temperatures (600°C.
evidence that the country rocks were onlyj or small satellitic stocks related to large vol- or lower). This interpretation is satisfactory
moderately warm and at shallow depths all umes of rock will commonly show chill zones for many porphyritic intrusives with an aphathe time of emplacement. Zoning of associated] •or porphyritic characteristics. Many large nitic matrix, but we need more data to be sure
mineral veins on a regional scale is common,i K masses or later members of a composite stock it is appropriate for plutons of almost excluas are veins of epithermal or xcnothermalj ,or batholith show no chill zones. There is sively phaneritic rock. Most plutons of the
character in the upper part of the epizone-j L^often a set of late-stage aphanitic or porphyri- epizone do have accompanying evidence of
Zoning of veins by repetitive introduction oij |tic dikes. Associated lamprbphyre dikes are contact metamorphism and contact metasolutions of diverse compositions during re-l lalso common. Distinct pegmatite veins are somatism. Andalusite is developed in shales
peated structural reopenings is common.1 litypically rare or minor although small pegma- and wollastonite locally in limestone at many
Peripheral outward deformation of the sidy ^.titic nests may occur locally. Aplitic veinlets contacts. Pyroxene intermediate between hewalls is a feature of some epizonal plutons.! imay be present, but aplite dikes or facies are denbergite and johannsenite is not uncommon
I t ranges from locally strongly deformedl jnot commonly abundant in the stocks. In (Allen and Fahey, 1957). Tourmaline is common
peripheral folds to gentle, parallel peripherajl ^some of the batholiths, however, aplite or in many aureoles of epizonal stocks. Many
folds; outward thrusting is inferred in onel equivalent alaskite may be well developed, epizonal stocks have at least local miarolitic
example; rarely there is a local thin zone al as in the Boulder, Seagull, and Ackley (White, facies, and they may be phaneritic throughout.
foliation or local thin layer of slight plasliq 1940) batholiths. Miarolitic structure is com- These facts are consistent with the probability
crystalline flowage in contact-metamorphia 1^ mon, especially in leucogranite or alaskite, and that the liquid phase of the magma of such
zones or local minor drag folding. Most of thy I it may have pegmatitic facies associated lo- plutons was relatively fluid because of its
plutons are small, but there are also neverthe Ifcally. Many aplite dikes are restricted to tlie content of volatiles during part or all of its
less many batholiths. The Paleozoic While] border zone of the pluton where they occur period of crystallization. An excellent comMountain batholith in New Hampshire assofj both in the. roof and in the adjacent igneous parison of the characteristics of highly viscous
ciated with cauldron-subsidence origin has anj .rock. Relatively flat-lying sheets of alaskite and less viscous magma emplacement in sills
outcrop area of 680 square miles, the Upper! I occur in tlie Seagull batholith, Yukon Terri- has been given by Tweto (1951).
Cretaceous Boulder batholith an area of 12003 tory, and of micropegmatite in the batholith
In a few examples the smaller plutons are
square miles, and the Tertiary Cordilleraj of the Casto quadrangle, Idaho.
accompanied by a small amount of breccia
Blanca batholith of Peru is more than 75|
Granophyre may also occur locally as whose origin is in part interpreted as an explomiles long, (Egeler and De Booy, 1954). Thy sheets, stocks, domical roof facies of stocks, sion breccia and in part as due to upward
emplacement of stocks and batholiths assM or as metasomatized country rock. Grano- drag of magma. Examples are a breccia of
ciated with'ring-dike complexes and cauldr(qj phyre, in general, occurs exclusively in tlie slightly rounded fragments of sedimentary
subsidence is uniformly attributed by
epizone.
rocks and of porphyry, in a matrix of similar
authors to subsidence, either subcolumnay
Occasionally stocks of the epizone may be ac- comminuted rock associated with a diorite
block sinking or block or piecemeal sloping. ^ companied by satellitic laccolitlis (Hunt, 1956; stock in the La Plata district (Eckel, 1949, p.
Reference for comparative purposes may b^ Strobell, 1956).
39) and breccia zones on one side of a granomade to the Cenozoic Slaufrudal stock 2
Emplacement predominantly by metasoma- diorite stock (Goddard, p. 383-384). Tweto
71^ kilometers in diameter, that cuts basalti^ tism is uncommon in the epizone and will be (1951, p. 526-528) has described an intrusion
lavas with intercalated rhyolitic volcanicl discussed under the title Pseudo-igneous Em- breccia as an advance guard of porphyry sills,
rocks in Iceland. Cargill, Hawkes, and Lede-i placement. Several plutons, however, do have formed by explosive intricutsion of fluids or
boer (1928) describe the stock as consistii^f an extensive aureole of granite or granite tenuous magma. The breccia may consist of
of miarolitic granophyre, in part with granilKJ gneiss resulting from granitization of sand- fragments of country rock and of chilled portexture. They suggest that the stock was] stone or metaquartzite. Contacts of pluton phyry in a shale matrix or of dirty contamiemplaced by sinking of the replaced maaj and country rock are normally sharp.
nated igenous material.
"en bloc" and that a distinct semihorizonUl!
Oftedahl (1953, p. 71-74,'92-93) has interThe magmatic origin of many salic dikes,
layering of the intrusion indicates intermittent, preted the central nordmarkite and monzo- stocks,, and laccoliths emplaced in the epizone
subsidence, the stock growing by the additimi tnite facies of the central part of the Sande is indicated by the inclusions of deep-seated
of successive sills or caps. Relations are e x c ^ pstock in southern Norway as the product of
Precambrian rocks which they contain where
tionally well shown in stefep topography.
•^assimilation of. lavas by an ekerite magma emplaced in overlying beds. Examples are the
Many other stocks and batholitlis have*! •more or less in place.
quartz diorite porphyry laccolith described
domical or a broad arch-shaped roof. ThisBj ^ Such criteria as lack of contact metamorph- by Rouse (1933, p. 145-146) emplaced in
commonly due in part to angular stepliBj ism and contact metasomatism, lack of chill Tertiary volcanic rocks with inclusions of
transection of the roof to yield this kind <H zones, and the presence of evidence for upward Precambrian rocks which have been brought
shape, in part to doming of the roof cither OT drag of wall rocks have been inferred (Read, up for a minimum of 2}^ miles, the inclusions
simple doming, or by doming accompanied I7J 1951, p. 9-10; Tweto, 1951; Hunt, 1953, p. of Precambrian rocks in monzonite-diorite
faulting in the roof due to distention.
165- Drewes, 1958, p. 233; Mackenzie, 1958, porphyry stocks, sills, and sheets emplaced in
680
A, F, BUDDINGTON—GRANITE EMPLACEMENT
Mesozoic beefs described by Eckel (1949, p.
34, 41), an example cited by Powers (1915, p.
166-168) in Vermont where bostonite dikes in
Middle Ordovician shales contain inclusions
of underlying Precambrian rocks, and similarly
that by Buddington and Whitcomb (1941, p.
78-79) from New York where small laccolites
and sills of quartz bostonite and rhyolite '
porphyry emplaced in Ordovician shales
•contain fragments of underlying Cambrian
sandstone together with rare fragments of
Precambrian basement material.
Some of the Tertiary laccoliths are so closely
associated with volcanic rocks that they can
confidently be considered to belong to a volcanic association. Hunt (1956, p. 43) writes
concerning the laccolithic mountains of the
Colorado plateau that "it seems likely that
most of the larger stocks in the laccolithic
. mountains reached the surface and erupted,
although probably none of them extruded any
great quantity of lava or pyrodastic materials".
A paper by Rouse el al. (1937) also portrays
probable relationships between laccoliths and
volcanic rocks. The major bodies originally
described by Gilbert as laccoliths are now
interpreted by Hunt (1956, p. 42-45) as the
upper part of stocks, the latter up to about 2
miles in diameter. The Three Peaks laccolith,
Utah; about 5 miles in diameter, has been
studied in detail by Mackin (1947). He finds
that the Upper Cretaceous (?) laccolith was
emplaced under a cover that ranged from 2000
feet to a possible maximum of 8000 feet. The
laccolith consists of quartz monzonite porphyry,
generally holocrystalline but with some glass
in the groundmass near contacts. He infers
that the chilled borders and the glass prove
that the mass was emplaced as magma. Some
of the quartz monzonite porphyry is finely
miarolitic.
The numerous diorite and monzonite porphyry sills of the La Plata district (Eckel et
al,, 1949, p. 34) also belong among the volcanic
bodies.
Granitic Stocks and Balholillis Associated
wilh Ring Dikes and Cauldron
Subsidence
'' Ifdroduclion.—Granitic stocks and batholiths associated in time and space with ring
dikes and cauldron subsidences in direct relation to volcanic rocks occur in many different
belts_,of_^fferent and widely spread localities
'
"--"'"^-.Dertinent to our
681
PLUTONS OF EPIZONE
are also independent larger discordant plutons,| K depression. Ross (1955) has pointed out that
associated with those directly due to cauldronj «pyrodastic rocks of rhyolitic, dad tic, quartz
subsidence, and inferred to be emplaced byi flatitic, and sorne of latitic compiosition are
block foundering or sloping. The prototype! ^present in many regions of the world, in volof this kind of complex is the Devonian Glenl «times which dwarf many batholiths. Larsen
Coe cauldron subsidence and the associated! land Cross (1956, p. 94) have estimated that
Starav granite batholith described by Cloughj i.lhe Miocene Potosi volcanic series of the San
cl al. (1909). Other examples of discordant! Huan volcanic rocks in Colorado contains 2300
batholithic intrusion following ring dike andj 5 cubic miles of rhyolitic volcanic rocks and 3000
stock emplacement are the Conway granite] f:cubic miles of quartz latite volcanics. The
pluton of the White Mountain batholith! trhyolite volcanic rocks are the equivalent of a
complex (680 sq. miles. Fig. 2), the Drammenl ^granite batholith 230 square miles in area and
and other batholiths (Fig. 3), and the Jos-| (10 miles deep. Stocks of monzonite and granoBukuru pluton complex (285 sq. miles) ofl Fdiorite emplaced in the same general period of
northern Nigeria (Jacobson el al., 1958, p, Hij II',time as the Potosi lavas are associated with
: them'and range in size from necks up to plutons
PI. vn).
Billings (1943) writes that he found de-| [2 by 5 miles in diameter.
Late Tertiary cauldron stdtsidence and intruscriptions in the literature of 115 ring dikes anda
30 ring-dike complexes. He states that 11 ofj jtsiim.—The youngest cauldron-subsidence comthe 30 ring-dike complexes have a central block! Cplexes may be expected to be among the least
of volcanic rocks that has subsided. TheseJ Eteroded and give the dearest evidence of becentral volcanic rocks are flows and pyroclasticj longing to a volcanic association.
Two such complexes from the United States
rocks ranging in composition from basalll
through andesite and trachyte to rhyolite|l 'will be described.
MEDICINE I.AKE HIGHLANDS CALDERA, CALIthey are, he believes, comagraatic with the?j
rocks in associated ring dikes. He further-i ; FORNu: Where erosion has not cut too deeply,
states that 17 of the 30 ring-dike complexesj * cauldron subsidences occur at the surface as
in the Pliocene(?)-Pleistocene(?) volcanic rocks
possess what may be called a central stockjj
and the central stocks usually consist of quartz-i I' of the Medidne Lake Highlands, California,
desaibed by Anderson (1941, p. 358-361).
bearing rocks, commonly quartz syenite or^
The caldera is an elliptical area about 4 by 6
granite. Belts in Nigeria and Southwest AfricaJ
miles in diameter in a shield volcano of platy
and examples elsewhere have been describedj
since Billings wrote so that many more ring-^ • olivine andesite about 20 miles in diameter.
The rim of the caldera is outlined by nine
dike complexes are now known.
volcanic vents from which platy andesite
Examples have been choseri from the litera^
(±10 per cent normative quartz and ± 6 1
ture to exemplify the foregoing principles!
per cent calcic oligodase) has issued. The floor
Before presenting these we might refer tol
of the caldera is inferred to have sunk at least
some of the largest masses of acid volcanicl
rocks which are believed to be of magmaliqj [i.SOO feet through coUapse of a central block
coincident with ring-dike intrusion and the
origin.
eruption of andesitic lavas squeezed up the
The volcano-tectonic depression . of the|
marginal fractures. This hypothesis would
Rotorua-Taupo graben in New Zealand (Mar-f
necessitate a stock of magma below with the
shall, 1935) is about 60 by 15-20 miles in arealt
composition of a quartz diorite. Later lavas
dimensions, with several thousand feet.off
depression and about 2000 cubic miles ofl [.'from the vents indude olivine andesites, dawelded tuff (ignimbrites) occupying a basiaj [-icites, and rhyolites and are inferred to represent
continued differentiation products discharged
of approximately 10,000 square miles. Thbl
would be about equivalent t o ' a batholith oil 11 trom later local vents in part spaced along
the margin of the depressed block. This would
200 square miles and 10 miles depth. Againl
Westervelt (1952, p. 565) has described a f,imply ^in part the existence, of magma below
jwhich could yield granitic masses on consoliMiddle Pleistocene rhyolitic tuff blanket in «|
jdation. The nature and tectonic relationships
fault trough in the Lake Toba area of NorlhJ
Sumatra covering 25,000 sq km and with al riof these volcanic rocks may be considered as
hsurface manifestations of ring-dike complexes
volume of 2000 cu. km. These are inferred tol
have formed as a result of the initial break'1 |- and associated deeper stocks and batholiths.
SiLVERTON CALDERA, COLORADO: Another
through of a comparatively shallow acid magmal
dera, described by Burbank (1941). The SUverton caldera is a minor unit areally and
structurally of the volcanic field of the San
Juan Mountains. The caldera was formed in
the late Tertiary by gradual downwarping and
faulting of a large shield-shaped block of
crust about 8 miles in diameter. As downwarping of the basin became accentuated with
thickening of the volcanic accumulations, ring
faults and associated radial fractures - developed. Intrusive bodies forced their way upward
along certain more strongly accentuated regional rifts, and great numbers of smaller
intrusive bodies and volcanic pipes penetrated
the broken rocks of the fault ring. Burbank
suggests that both the rock alternation and the
concentration of intrusive bodies indicate that
at moderate depths below • the surface the
margin of the caldera is underlain by a more
or less continuous ring of intrusive rock. The
intrusive rocks consist of gabbro-diorite,
andesite, latite, quartz latite porphyry, and
rhyolite. The volcanic rocks consist of andesite, "latites", quartz latite, and rhyolite.
Larsen and Cross (1956, p. 227) describe one
of the quartz monzonite stocks as 2 by 5
mUes in diameter.
Early Tertiary cauldron subsidence and plutons.—Early Tertiary plutons associated with
cauldron subsidence may be expected to
indude some which have been eroded to a
deeper level than those of the Late Tertiary,
and this is the fact.
QUITMAN COMPLEX: The following summary
of the Early Tertiary Quitman complex is
based on that by Huffington (1943). A series
of lava flows ranges in composition from basalt
to trachyte and rhyolite; rhyolites are most
abundant. They are associated with pyrodastic rocks, and the whole has an approximate
thickness of 3500 feet. Late basining, probably
due to magmatic subsidence bdow the volcanic
rocks, has dropped the central portion of the
volcanic rocks approximately 4500 feet. A
discontinuous elliptical ring of intrusives
around the volcanic rocks is interpreted as a
ring dike about 4 miles in diameter. The earliest intrusion in the area -was a diorite; the
ring-dike intrusion averages quartz monzonite.
There is a rdated stock of quartz monzonite
adjacent to the ring dike. The quartz monzonitic stock is subcircular -with a diameter of
about 3.5 miles and is separated from the parts
of the, ring dike by a septum about half a
mile wide of Lower Cretaceous sedimentary
rock. B e l t s
of
anlite
and
irriinilA r.n,.r.U,,..,,
TnTTONSTJFTPIzoNE"
granite and granophyre form 63 per cent of the siliceous facies of the nordmarkite. The volMea of intrusive rock in the belt of Tertiary" canic rocks seem to have settled at least 5000
plutonic complexes of the British Isles, gabbro feet and probably at least 17,000 feet in one
and dolerite 33 per cent, and ultrabasic rocks area since they do not occur in the adjoining
region. The emplacement of the batholith is
3 per cent according to Richey (1948, p. 55).
inferred to result from roof subsidence. Magma
NEW HAMPSHIRE BELT OP MISSISSrPPIAN(?)
PLUTONS: The ring-dike complex of the Ossipee moved upward along great fractures and issued
Mountains, New Hampshire (Kingsley, 1931), at the surface as great flows and pyrodastic
EXPLANftTION
has
one of the most nearly perfect ring dikes of deposits.
MISSISSIPPlftN
The belt of epizonal plutons is slightly disthe New Hampshire belt and exemplifies the
WHITE MCXWTflIN PLUTOWC-VtJUaNlC
scstts
general character of the complexes (Fig. 2). cordant to the trends of the older country
The ring dike is described as subcircular with a rocks.
OSLO BELT OF PERMIAN PLUTONS: T h e O s l o ,
diameter of a little more than 8 miles and is comGronile oilh hotliflgtite,
posed of porphyritic quartz nordmarkite (13 per Norway, belt of cauldron subsidences or ringcent normative quartz). Within the central com- dike and central complexes has been described
Oonitt [!Q>phri|
plex is an arc-shaped mass of the Moat vol- by Holtedahl (1943) and Oftedahl (1952;
canic rocks. These have an approximate thick- 1953). I t is of such general significance that
Ouorll Jyenllc
ness of 7000 feet and consist of basalt (4 per the writer cannot refrain from induding a
Syinlll ( 1 , 1 ;
kcent normative quartz), andesite (13.4 per summary here. (See also Figure 3.) The pluNtphlllni lytntK ( n i l
imuil
cent normative quartz), and quartz porphyry tonic complexes were emplaced in a lava
vp"ti<»t
Moat volconlcl
flows, and equivalent tuffs and breccias. The plateau consisting of 2000-3000 m of basaltic
F ^ , t T , ^ A lEttrullva phoit ol
WhtK Mcun(o<notutan(c-«Qlcontc t t t t t t l .
iemainder of the central complex, except for a and rhomb porphyry flows. The plutonic phase
riowi, tgrftORdbrtccfoi; rhyoliti, baton,
,5niall block of country rocks, is composed of a began with the consolidation of larvikite
onde4lte,ond tom* Irochylc.
Coarse-gained biotite granite (25.8 per cent plutons, tlie magma of which corresponds to
? UPPER DEVONIAN
normative quartz). Kingsley estimates that the that of the rhomb porphyries. During later
M£W HAMPSHIRE PUlTOMlt SERIES
minimum subsidence of the volcanic rocks periods, with the formation of syenitic and
Pr«do*nlr«nlly ouotll
.on the borders is 4500 feet and in the center granitic stocks there occurred the cauldron
monioniti o r i quorli
d'Orite, qencrolly totloled.
'il2,500 feet. The biotite granite is inferred to subsidences. Quartz porphyry annular dikes
have been emplaced as a result of either piece- occur in three of the four described cauldrons
SILURIAN ANO LOWER DEVONIAN
meal stoping or a columnar-block subsi- as an early phase of intrusion.
PredoTiliio/i]), LoMti
SO
The Oslo belt is very instructive because of
(dence.
Ocvonlon m'coceogs
quortilit and mica lehlUl, loco)), qranMe
I The White Mountain batholitli (fig, 2), the association of large batholiths of larvikite,
qnelu and Khistt tal(hq(Onll(c ln]ect>Qn.
another member of the New Hampshire central nordmarkite, and biotite granite which form
;Complexcs, is significant because of its size. a belt about 200 km long; the four major caulfjThe following description is condensed from dron complexes lie within the central part of
FIGURE 2.—NEW HAMPSUIRE BELT OF PLUTONS
iilhat of Billings (1928), The batholith lies this b d t (Oflendahl, 1953, Fig. 1). One of these
Ossipce complex ring dike and biotite granite stock of cauldron subsidence; White Mountain bathv, [Vbout 4 miles north of the Ossipee Mountains batholiths, tlie Drammen biotite granite (Ofteolith of cauldron subsidence and coalescing rim fracturing; both Mississippian (?) of epizone; and oldei, ^
Winnipesaukee batholith of transitional (?) mesozone-catazone; Modified after M. P. Billings, 1956,'? ,tomplex. I t underiies about 680 square miles dahl, 1953, p. 103), encloses the Drammen
N . H . Planning and Development Commission, Division of Geol. Sci., Harvard University and U. S:-i '..and consists predominantly of granite witli cauldron in the form of a huge cylindrical
block or roof pendant. The biotite granite
Geological Survey
•'': subordinate nordmarkite and great blocks of
volcanic rocks, from a few to 8 miles in diam- magma is younger than the rocks of the cauleter, that have settled into the batliolith. The dron, and the stoping followed the ring fault
Permian, Mississippian{?), and Devonian dikes they range in size from small plugs and
plutotis associated wilh cauldron subsidence.— dikes to batholiths underlying as much as 5 volcanic rocks consist of siliceous flow rocks nearly exactly. I t has a quartz porphyry
Four.great belts, three of them more tlian 680 square miles. The rocks of these bells .and interbedded tuffs and breccias to a thick- border against the effusives of the Drammen
ness of about 11,800 feet. The siliceous flows cauldron. The Drammen pluton is about 55
200 miles long, each with numerous granitic may be thought of as representing in part
are largely comendites (24-33 per cent norma- km long. Against the rocks of tlie Giltrevann
stocks, batholiths, and ring-dike complexes levels of deeper erosion than the Tertiary
in direct tectonic, geographic, and time rda- plutons and in part the rise of large masses of ^ tive quartz) or quartz porphyries. Trachyte cauldron it has a border facies of quartz porI (18.3 per cent normative quartz) also occurs. phyry with an aplitic groundmass. Oftendahl
tionsliips with volcanic rocks of related com- granitic magma to relatively high levels.
(1953, p. 58) further suggests that the granite
'
Chapman
and
Williams
(1935,
pr
507)
find
.[The plutonic phases indude a small mass of
positions, have been described in recent years.
diorite, nordmarkite (4-13 per cent normative magma was at a rdatively high temperature,
The belt of Tertiary ring dikes and caldera that granite forms more than 78 per cent ol
the plutonic complexes of the New Hampshire, quartz), and granite (23.6-28.5 per cent norma- perhaps superheated. An ekerite batholith is
subsidences with associated granite stocks of
tive quartz). Some nordmarkite porphyry younger than the rocks of the Sande cauldron.
Scotland should also be noted. The four belts belt, syenite and quartz syenite 20 per cent;'
and
gabbro,
diorite,
and
monzonite
less
than
2;
occurs
as small satellitic stocks or as chilled The ekerite is full of pegmatite nests and has a
indude that of New Hampshire (Billings,
1945; 1956) of Mississippian(?) age, the Oslo per cent. Jacobson cl al. (1958, p. 7) estimate'^ border facies whose groundmass is dense. I t is porphyritic border zone. Holtedahl (1951,
district in Norway - (Hoitedahl, 1943; Ofte- that granite forms 94 per cent of the plutons of| noteworthy tliat the extrusive comendites p. 90) condudes with respect to the mechaare comparable to the plutonic granite and nism of emplacement of the batholiths that
dahl, 1953) of Permian age, a belt in Nigeria the belt in Nigeria and mafic to intermediate
the extrusive trachyte to the plutonic more "huge subterranean crustal blocks sank tn nn
—fr;reemv.o.od, 1951; Jacobson et al., 1958), rocks only 6 per cent. By way of comparison
monzonite. Granites form less than 10 per
cent of the plutons, and monzonite and syenite each about 10 per cent. The ring dike is
• inferred to have been emplaced in large part
by stoping along the ring fracture.
and one of late Karroo age in Southwest Africa
(Korn and Martin, 1954). These plutons
occur in the "epizone" of the crust and can
approximately be considered to belong to a
volcanic association. In addition to the annular
683
684
PLUTONS OF EPIZONE
685
loiknown depth along curved fracture lines, stock about 17 by 27 km in diameter, in Fin»ith magma occupying the vacated space". land, The following summary is based on the
Oftedahl (1952, p. 58) infers a monzonitic work of Savolahti (1956). The earliest intru•lagraa batholith at least 100 km long and 20- sions form an arc and consist of several succes^ km wide, slightly superheated, to explain sive intrusions of gabbro with anorthositic
ike rhomb porphyry lava flows. He further differentiates. The younger gabbro intrusions
suggests (1952, p, 60) that stoping normally have chilled contacts against the older. The
»as arrested dose to the surface (about 100- main core of the complex is a stock of biotilic
500 m below the surface), but occasionally the rapakivi granite. The youngest intrusions are
magma stoped its way dear to the surface to granite porphyry dikes with fine-grained facies
fcrai areal eruptions.
in contact with all older rocks. Savolahti (1956,
p. 83) writes of the rapakivi granite in general
that "At an early period the hypabyssal, partly
'Stocks Primarily by Cauldron Sidisidence,
effusive characters of rapakivis were described.
but Accotiipanied by Oulward or
Likewise, the occurrence of miarolitic cavities
Upward Pressure
was recognized to be typical, and the scarcity
General discussion.—^The preceding discus- of aplites and pegmatites .was known". The
ion has dealt witli stocks that are assumed to stock is in general discordant to the country
liave been emplaced effectively by subsidence rock which consists of migmatites and older
iif columns pr blocks. There are a few examples microdine granite, but locally the trend of the
jn which subsidence of blocks or columns is foliation of the migmatites has been deformed
.nferred to have been the major mechanics into conformity with the boundary of the infi emplacement, but they are also accom- trusive complex. Some of the rapakivi granites
panied by evidence of deformation of country in this region have been determined by Kuovo
k due to outward side pressure or uplift of and Cast (1957, p. 30) to be about 1650 million
years old, on the basis of Rb-Sr, K-A, and U,
ml
The basaltic lavas around the Mull complex Th-Pb.
(Bailey et al., 1924, Chapters X I I and XIII)
show several concentric folds with dips of
Other Discordant Plutons of Epizone
l0''-30° in discontinuous arcs or cirdes.
Introduction.—The characteristic setting for
lyrrell's description (1928) of the northern
franite mass of the island of Arran, Scotland discordant batholiths associated in space, time,
shows that along one part of the border the and tectonics with ring dikes, cauldron subtountry-rock schists have been dragged around sidence, and stocks is a peneplaned surface on a
W an uplift produced by the granite magma so "basement complex" or series of folded and
,lhat their strike swings into approximate par- faulted beds overlain unconformably by a vetllelism. In another part of the border there neer of lavas. Such plutons occur in the New
as been upward movement by faulting and Hampshire, Oslo, Nigeria, and Southwest
Africa bdts and the Glen Coe district that have
nylonitization.
IT Mt. Monadnock, Vermotd.—The Mount been referred to. They may be very appropriMonadnock pluton in Vermont is inferred by ately called subvolcanic. Although many stocks
Chapman (1954) to result from the settling of a and batholiths are thus either directly or intemical reservoir which developed cylindrical direcdy associated with cauldron subsidence
uid radial fractures with consequent cauldron and ring-dike complexes, many plutons of the
lubsidence and stoping of large arcuate-shaped epizone are not, although they are in general
» » dabs as the major method of emplacement. discordant. Many of these latter plutons are
-(<(j iNorth and south of the stock, however, quart- associated with volcanic rocks in space and
;jites and schists which in general strike about time, but the evidence is commonly not suffinorth and dip east have been strongly twisted ciently direct to tie both assuredly to tlie same
wd their schistosity thrown out of regional tectonic history. Some of these plutons may not
strike. Chapman suggests that during the very. have had connections that broke through to the
Jarly stages of intrusion positive magma pres- surface to yield lava flows. Others probably did
FIGURE 3,—OSLO REGION, NORWAY
ide was sufficiently vigorous for a brief period have such connections, but the roof either reFour Permian complexes (B, D, 0, S) of lavas, ring dikes and stocks of cauldron subsidence,
of time to deform the immediately surrounding mained intact or broke down and sank in the
-f.H_voimEer_discordant batholiths; all of epizone. After Oftedahl (1953)
mapma in such a wav thaf Hirprf rnnnprfinn hptietamorohic rocks.
I L U l U i U U^HWHJWff
mF
associated with present evidence for caldera the Bohemia district (Buddington and (Callasubsidence. >
ghan, 1936, p. 426) the intrusions occur in an aitjj
The Bayview and Packsaddle Mountain and as radial dikes. The line of intrusions has al
stocks, Idaho, described^ by Sampson (1928) general northerly trend, but the individual in-|
possibly afford a link between the directly sub- trusions and veins trend mainly to the west orj
volcanic type of pluton and plutons not now northwest. Epithermal and xenothermal metal<|
associated with volcanic rocks. The stocks are liferous veins are associated with the stocks.!
predominantly granodiorite and are significant An extension of this belt into Washington isj
because probably subsidence of roof rocks has shown on the map by Waters (1955, PI. !)•
accompanied their emplacement. The stocks
A belt of Quaternary and late Tertiary voll
are discordant with the relatively flat lying canoes lies in general to the east and roughl/
structure of the surrounding rocks, which are parallel to the line of older Tertiary intrusirtj
predominantly the Precambrian "Belt" series stocks.
of sedimentary rocks. Block faulting has reSnoqualmie balholith,
Washington.—1
sulted in downdropping of blocks of Cambrian Snoqualmie batholith of Washington (Fig. OJ
sedimentary beds. The block faulting is found of early Miocene or late Oligocene age (Grant,!
only about the stocks and is related to the in- 1941, p. 590-593) has been described by Smilhl
trusion. The Cambrian rocks are found only and Calkins (1906), I t is composed of granodiwj
EXPLANATION
where they are more or less engulfed in igneous ite and biotite granite, is miarolitic (WateM
rock. The granodiorite is coarse-grained up to 1955, p, 711), and has porphyritic modifies^
contacts. The collapse structure, recalls that tions on the margins of large masses and ini
associated with cauldron subsidence. There is dikes. I t is emplaced in folded sedimentai
no pegmatite in the granodiorite, but there are , beds and in the Keechelus volcanic rocks, Thej
W
a few aplite dikes.
latter are in part gently folded and in part havi
Late Terliory and
An excdlent example of control of emplace- only initial dips. They consist of pyroxo
Ouoternory Volcanoes
ment of a Precambrian quartz monzonite stock andesite, dacite, rhyolite, and basalt with
ond Volcanic cones
of fractures of the country rock has been de- first two greatly preponderating. An analysiso
scribed and mapped by Steven (1957, p. 365- a sample of the andesite shows 18 per cai^
375). One border has many angular step-like normative quartz and is very similar in coi
(?) Lole Miocene Intrusive
irregularities, and another has a zone 1.5-2 position to the granodiorite which intrudes ilj
igneous rocks
The batholith is about 10 miles in diameter t
miles wide with a complex network of dikes.
Several stocks or lines of stocks and several is inferred by Smith and Calkins to have (
batholiths of the epizone will be summarily solidated about 4000 feet below the surf*
Mesozoic igneous
described. These may be either parallel or dis- Knopf (1955, p. 695) states that tlie batholiU
intrusives
is roughly 250 square miles in exposed area t
cordant to regional structure.
Stocks and volcanic rocks of western Cascade may be the top of a mass 4000 square miles i
Mountains, Oregon.—The Miocene (?) lavas extent not yet uncovered by erosion.
Poleozoic and Mesozoic
and the'line of Miocene (?) intrusive stocks of
Balholilli, Casio quadrangle, Idalto.metamorphic roclts
the western Cascade Mountain range in Oregon Miocene batholith described by Ross (19i^
(Callaghan, 1933; Buddington and Callaghan, from the Casto quadrangle, Idaho, is also not^
1936) afford an excellent example of an associa- worthy because of its size. It is at least 30 mO(^
tion of lavas and plutons of similar composition, long and averages 7 miles wide. Much the ma
and of association in geography and time (fig. abundant rock according to Ross is graniU
4). The belt about parallels the trends of the but there are small masses of quartz monzoniti^
substructure. The lavas range from basalt to granite porphyry, dacite porphyry, qua
rhyolite but are characterized by andesite. The diorite, and granophyre. The batholith di^
intrusive stocks in Oregon occur at intervals 01igocene(?) volcanic rocks composed
along a line about 200 miles in length. They ponderandy of rhyolite and quartz latite, an^
/?«•
75,.
range in size from small plugs to a stock IJ^ by Ross states that some of the late rhyolitic flff
FIGURE 4.—BELT OP TERTIARY INTRUSIVE STOCKS EMPLACED IN VOLCANIC ROCKS OF WESTERN
2}4 miles in diameter. The rock of the smaller may possibly be related to members of
CASCADE MOUNTAINS IN OREGON AND WASHINGTON
bodies is generally porphyritic aphanitic, that pluton. The depth of intrusion he infers to hiiV"
Modified after Tectonic Map of United States, Am. Assoc. Petroleum Geologists, 1944
'of the largest body is even-grained granular. been not much more than 2 miles. The gramtJ
The rocks range in composition from augite is locally finer-grained dose to the conti _
Jroad low arch by the granite rather than cross- occurs in a belt extending from a little northdiorite through augite dacite porphyry and and granite porphyry may be a marginal faotj
[cut. The granite locally has followed faults. west of Boulder to the San Juan district in Colaugite granodiorite porphyry to granite. The Micropegmatite occurs in nearly horiamO
J. Boulder-San Juan discordant belt of pinions, orado (Fig. 5), a distance of about 200 miles.
larger masses are in general more siliceous. In ribs. The overiying strata were domed intw
V^olorado.—A series of plutons of Tertiary age The belt is strongly discordant to the regional
'i>.ru-»j,ic r / l v i r L A U t M E N I "
Structure. Among others it indudes the Jamestown, M o n t e z u m a , Silverton, and L a Plata
stocks and the M o u n t Princeton batholith.
Lovering a n d Goddard (1950) have described
the b d t . T h e y s t a t e t h a t some stocks probably
689
PLUTONS OF EPIZONE
lies perpendicular to the direction of Lararaide
The T e r t i a r y M o n t e z u m a q u a r t z monzonite
compression, it is possible that tensional forces ot
some magnitude were present here during the^ ''ode is an example intruded discordantly in
folding of the region. The belt of porphyry stocki" the epizone almost exdusively in Precambrian
occupies a position on the northw.estem side ot a
tectonic transition zone between two 1)^)68 of
significant because t h e great rdief a n d mine
workings permit a n accurate picture of their
shape and geologic relationships. T h e y a r e
EXPLANATION
TERTIARY
EXPLANATION
Tog
Agglomeroles
V
V V
V
V
V *
Tg
Tertiary
intrusive bodies
V
V V
Gronodiorile
CRETACEOUS AND JURASSIC
SJV
Terliory
volcanics
w.
Precombrion
igneous ond
metomorptiic
rocks
^
Predominontly limeslone
(Representotive formation boundories
indicated)
X.60
Strike and dip of bedding
70'*».
Strike ond dip of overturned beds
109'
toa'
107'
lOS'
/Oi'
104'
Foult
FIGURE 5.—BOULDER-SAN JOAN BELT OF PLUTONS DISCORDANT TO REGIONAL STRUCTURE, COLORADO,
Modified after Geologic Map of United States, U. S, Geol. Survey, 1932
occupy old volcanic throats, b u t many others
were roofed with pre-Denver (Upper Cretaceous and Paleocene) rocks and probably forced
their way in by stoping and intrusive faulting.
T h e earliest intrusives show structure concordant with the country rock much more commonly than do the later, and among the latest
of the intrusives explosion breccia is common.M o s t of the intrusives lie between monzonite
and q u a r t z monzonite in composition. T h e
stocks a r e associated with dikes a n d sills. T h e
texture in general ranges from coarse porphyritic and medium-grained to porphyritic aphanitic. T h e intrusion continued intermittently
throughout the considerable span of time during
which the Laramide revolution Was in progress.
Local transverse fracture zones marked by intrusive activity followed a period of regional
northwesterly folding and faulting. T h e transverse structure is explained as follows;
(Lovering atid Goddard, 1950, p . 63).
regional deformation. Fault 'movements in tie]
porphyry belt suggest that the northern part ^
the transition zone was one of shearing with nearlyJ
horizontal movement as well as one of tension. III
is believed that these two stresses—shearing andj
tension—were in part responsible for the rise ofj
the magma that formed the porphyry stocks,"
Dings and Robinson (1957) have desaibed
the M o u n t Princeton batholith which is one
FIGURE 6.—TERTIARY GRANODIORITE STOCKS EMPLACED DISCORDANTLY IN EPIZONE
of the largest bodies in the belt. I t is about 14
In asymmetrical anticline of limestone, near Concepcion del Oro, Mexico. After Rogers, Tavera, and
by 19 miles. T h e y describe i t as quartz mon- Slloa (1956)
zonite with small areas of younger granite, ifc;
trusive q u a r t z monzonite porphyry, and quarU||is;gnj,^titg5^ schists, and gneisses (Lovering
emplaced discordantly in t h e core of an a s y m latite porphyry. Only l o c a l l y d o e s the rock of3^35^
metrical a n t i d i n e of Jurassic and Cretaceous
the batholith change texture to a'porphyry at 1 xhe mineralization a n d by inference some of
sedimentary beds. Limestones a r e p r e d o m i n a n t
the border, b u t apophyses arfe finer-gramed^jie associated plutons of the Boulder-San
with minor shaly limestone. T h e roof is faulted
Small aplite dikes occur throughout. Pegnia-^ i)iian belt has been stated (Eckelmann and
in a manner which m a y be explained as due to
tite dikes are rare. T h e younger granite, 1 fulp, 1957) t o be 59. ± 5 million years of age.
a slight doming by upward m a g m a pressure.
leucogranitic type, however, is locally miarolitiC| Stocks of Coticepcion del Oro, Mexico.—Two
Roof p e n d a n t s lead to a n inference of a relaand.has numerous pegmatite veins. Beryl occuis^ |osely adjacent granodiorite stocks of Tertiary
tively flat archlike roof with re-entrants. T h e
in the granite, the miarolitic cavities, and '
emplacement seems clearly t o be d u e to s u b ;e are well exposed northwest of Concepcion
pegmatite. T h e r e are two granite stocks, oiit]
• D r r , i n M » - : — f d - A\ T I
1--— '
TETTTTOSTJF-EPIZDTTF'
considered a "resister" to granitization. The
mineral deposits are zoned, in part with a vertical distribution, from hypothermal deposits at
lower levds to epithermal chimney deposits in
the higher parts of roof.
Boulder batltolilh, Montana.—A pluton of
Late Cretaceous age, of great size for the epizone, and presumably somewhat older than the
plutons of the Boulder-Breckenridge belts, is
represented by the Boulder batholith in Montana. Knopf (1948, p. 666) states that a great
volume of andesite and latite was erupted,
probably just before emplacement of the
Boulder batholith, which rose to such a high
level that it invaded the pile of lavas. Balk
(1937, p. 91) states that the Boulder batholith
approached the surface somewhere between
2000 feet and 10,000 feet. The batholith is 70
miles long with an area of 1200 square miles.
Grout and Balk (1934, p. 880) state that flow
structures are poorly developed and (p. 885)
that linear structures are much more widespread and uniform, and probably more significant than the foliation as indicating the intrusive movement, although they are also elusive.
Knopf (1957, p. 81) states that tlie batholith
is composite and—that the order of intrusion
is (1) basic hypersthene-bearing granodiorite, (2) granodiorite, (3) porphyritic granodiorite, (4) biotite adamellite, and (5) muscovitic
• biotite granite. Alaskite and aplite are abundant. Contact metamorphism has locally developed sillimanite - cordierite - microperthite
homfels. Knopf describes the emplacement of
the batholith as the problem of how five different magmas in turn made room for themselves
in the higher level of the crust and built up a
composite batholith. He writes that hear the
batholith the invaded country rock has been
more dosely folded than at a distance from the
contact. In places the strata adjacent to the
batholith stand vertically and have even been
overturned. Locally a series of reverse faults
has developed along the eastern border of the
batholith. The intrusive magma according to
Knopf has manifestly made room for itself by
crowding aside the enveloping rocks, by dose
• appression of the beds, by overturning them,
and by imbricate high-angle thrusting,
Knopf reports (p. 90) the age of the batholith
as determined by (ihc Larsen zircon method to
range from 62-72 m.y. and by the potassiumargon method, 87 m.y.
Seagull batholith, 'Fukon Territory.—The
based on his work. The batholith is about 6 by
28 miles and is emplaced largely in the trough
of a syndine of Paleozoic rocks (Fig. 7). The
batholith could be of mid-Cretaceous or Late
Cretaceous age. I t is in a deeply dissected
mountain country with great rdief and can be,:
shown to have steep walls and relatively flat
undulatory roof with several of the mountain
peaks capped with hornfels and the valleys in.quartz monzonite. The country rocks are re:
gionally metamorphosed and belong to the;
rauscovite-chlorite subfacies. There is no evi-*
dence for forceful intrusion or side thrusting.
The carbonate rocks have diopside, tremolile,^
and garnet in the contact zone, at one locality,;^
with wollastonite. The rock of the batholith is^!j
a coarse-grained leuco-quartz monzonite witH
flat sheets of fine-grained and porphyritic
alaskite. Alaskite in near-horizontal layers up
to 20 feet thick forms 5-25 per cent of the masiThere are miarolitic cavities in the quartz mon-,
zonite with quartz and tourmaline. Dense;
spherical aggregates of quartz and tourraalii*
aJso occur as replacements in the quartz mon-;
zonite and alaskite. There is no pegmatite. •?•
Precambrian Plutons of Epizone
General statement.—^The major types oi
epizonal plutons may be of Precambrian u
well as of Tertiary age. Discordant plutons of^
Precambrian age have been described by,
Anderson, Scholz, and Strobdl (1955) froo'^
the Bagdad area, Arizona, and by Kalliokoshj
from the Weldon Bay area, Manitoba. Other
types of Precambrian-plutons are referred ti^
below.
T
Granophyre.—Extensive granophyre sheas
associated with gabbroic or diabasic stratiform complexes have been described or re(fc-1
scribed in recent years from tlie Precambrian of <
Minnesota (Schwartz and Sandberg, 1940),;
Wisconsin (Lcighton, 1954), the Wichita Moun*',
tains of Oklahoma (Hamilton, 1956; Merrill
1958), and the Sudbury complex in Ontario
(Thomson, 1956). All these were emplaced 'm\
the epizone. Hamilton writes that in the^ ;
Wichita Mountains, granophyre, granite, and
rhyolite form a sheet complex of dozens of
separate plutons, of which many are sills and
funnel-shaped masses. He states that granil^j
and rhyolite may be either lateral equivalents
of granophyre or intercalations in granophyre,'
and that the granites are probably iri general^
younger than the granophyres. Rhyolite ii
"55r
ft, r . JIUJJULWUIUN—UKANlTJi JiMPLACliMliNT
cavities are common in one of the granite masses
and thaf it may have been emplaced as a batholith. A younger granite mass has chilled fades
against older rocks. The younger granite is
also miarolitic. K/A and Rb/Sr ages of a biotite
from the younger granite are reported by Merritt (p, 62) to be 480 m.y. and 500 m.y. respectively.
Thomson (1956, p. 43-45) has proposed that
the Sudbury Basin is a volcano-tectonic depression surrounded by a ring complex of dikelike and sill-like character, and that the granophyre (micropegmatite) was emplaced as a
ring structure inside the norite.
Ring-dike complexes.—The Ahvenisto pluton
of Finland has already been- referred to as an
example of a Precambrian ring-dike complex.
Two other ring-dike complexes, the ChathamGrenville and Rigaud stocks of probable Precambrian age in Quebec, have been described
by Osborne (1934). Chill facies such as quartz
porphyry and syenite porphyry are found in
both complexes, and miarolitic structure is
found in the syenite of the Rigaud stock.
Aureoles of Psetido-igneous Emplacement
Description.—^The contacts of the plutons
of cauldron subsidence are almost universally
sharp as are the contacts of most other stocks
of the epizone. Extensive metasomatism of
earlier gabbro members by younger granitic
magma, however, has been described by Korn
and Martin (1954) from the Messum complex
in southwest Africa. The Bingham, Cassia and
La Plata plutons in Utah, Idaho and Colorado
respectively have been interpreted as cores of
magmatic origin with aureoles of pseudo-igneous granite, the product of replacement of
quartzite or sandstone. Loughlin and Koschman
(1942, p, 41-42) have also described a small
body of granophyre interpreted to result (rom
metasomatism of sandstone by emanations from
an adjacent Tertiary granite body,
Bingham, Utah, slock.—Stringham (1953)
has described a small stock at Bingham, Utah,
where granite forms about two-thirds of the
area of the pluton and is inferred to be the
product of granitization of quartzite. Some of
this granite is exceptionally high in KjO. The
core of the stock is granite porphyry which is
interpreted to be of magmatic origin. In the
area to the south (Gilluly, 1932, p, 65) a series
of volcanic flows in which latite is overwhelmingly predominant are cut by intrusives inferred
--tn .be_ro,ughly correlated with the Bingham
"*
-~
"-'-^'"'rt/rpne.a.ffe.
PLUTONS OF EPIZONE
Cassia balholith, Idaho.—Anderson (193l)|over of rocks after folding and perhaps faulthas described the present 60 square miles a jg ^f ^],g Concentrator volcanic rocks (Creposure of the Cassia batholith to consist d iceous ?). He states that it is possible that the
about two-thirds porphyritic, usually gneissii iameVisi quartz monzonite and Concentrator
granite and one-third granodiorite. He bdieve „im„i^ ^^^^ represent the same magmatic
the porphyritic granite gneiss is a replacemen ^^^ -pj^g disregard of older structures by the
of meUquartzite and the granodiorite a cry* nlrusive, the absence of wall-rock structures
tallized magma. The batholith has a dome oncordant with its contacts, and the sporadic
shaped roof, and the metasomatic porphyriti jes^rvation of fine-grained (diilled) border
granite extends at least 1800 feet down, Th nies mdicatc that the intrusion took place at
batholith is of late Cretaceous or early Tertiai) i relativdy shallow depth. The weakness of
age. The data are not too definitive, but
eation in the rock is inferred by Gilluly to
batholith is here classified as emplaced in
icate that tliere was little motion in the
epizone.
gma at late stages of its consolidation. After
La Plata slocks, Colorado.—Eckel ( W |ls consolidation, however, it was fractured
has inferred the emplacement of small Lai long westward-trending fissures, and aplite
Cretaceous or Tertiary diorite and monzonil ikes'were injected in large quantities. Northstocks in the La Plata District, Colorado (Fij
rd-trending fractures followed and were
5) to be in part by replacement or assirailatia
pied by pegmatites in the apical part of
of country rock. He finds (p. 39) that wherc^ e stock. At later stages solutions chloritized
monzonite stock transects beds of sahdsti
id sericitized .the rocks of the apical part of
there arc inclusions from an inch to sevenjj le stock and deposited cupriferous and asso- '
hundred feet in length whidi retain the attitui
ted metallic minerals of the New Cornelia
and position of the beds from which tliey wei^ body.
derived. However, he also finds that in man] Banover slock, New Mexico.—The Hanover
places contacts between the diorite and moi
anodiorite stock. New Mexico, has been denite and the host rock are sharp and that tl^ bed by Paige (1916), Sdimitt (1933), and
diorite and monzonite locally contain frag err el al. (1950). Where emplacement has been
ments of Precambrian rocks even where thi :companied by uplift and outward deformaare in'Paleozoic or younger sedimentary
n. It is about 2.5 miles long, north to soutli,
id less than a mile wide. The Paleozoic bedded
s dip away from the stock on the east and
Supplementary Descriptions of Plutons
t flanks so that it has the relationship of an
Emplaced ifi the Epizone
tidinal structure. At tlie south the bedded
New Cornelia quartz, monzonite stock, j4f»-j s have been deformed into an overturned
zona.—The New Cornelia quartz monzoi
dine and an asymmetrical antidine beyond,
stock in the Ajo district of Arizona exhiWttJ e fold axes form arcs parallel to the edge of
many features characteristic of the Tertii
e stock as though the folds had been formed
stocks of the southwestern United States,
lateral pressure from the overriding stock,
following description of it is condensed f i ^ ically folding was so intense that thrusting
that by Gilluly (1946).
:urred on a low-angle fault plane. Kerr et al.
The great copper mine at Ajo is opened in tj 950, p. 301-302) state that the near-by
low-grade epithermal deposit of chalcopynl
nta Rita stock arched and cut through overand bornite disseminated in the New Corni
ing sedimentary rocks and quartz diorite
quartz monzonite tliat is tentatively referred
s.
Early Tertiary age. The New Cornelia stock
Marysville slock, Montana.—The developexposed over an area of about 6 square mfli
lent by Barrell (1907) of the hypothesis of
There is a discontinuous border facies consist
ck subsidence in magma as the mechanism
of fine-grained quartz diorite. The preponderant emplacement of the Marysville granodiorite
rock is an equigranular quartz monzonite wil^
has made the latter one of the dassic
a poorly developed linear structure,
mples of this phenomenon. Knopf (1950)
country rock is predominantly the Com
rites that the stock is 6 miles north of .the
trator volcanic rocks consisting of ande
Tthem end of the Boulder batholith and
keratophyre, and quartz kcratophyre floi
obably an outlying cupola. I t is only 3 square
breccias, and tuffs with highly altered and
iles in area. Barrell states that the roof sediplex structure. The Cornelia intrusion Gillt
Sents were domed over the granodiorite to the
infers_probably took place under a model
"tent of 1000 feet, possibly 3000 feet; that
w
faulting immediately preceded the invasion of
the stock caused by upward pressure of the
igneous mass; and that at numerous places the
roof of the stock passes beneath the sedimentary
cover at a flat angle. Barrell further writes that
the granodiorite maintains granularity up to the
contact and is medium- to coarse-grained but
becomes markedly more porphyritic in outlying
tongues and wedges. Aplite occurs within the
margin of the stock and in rocks of the border
zone but is rare in the interior. There is also
minor pegmatite in the same zones as tlie aplite.
Knopf comments (5950, p. 840-842) on the
remarkable contact-metamorphic aureole. The
argillites are converted to cordierite hornfels,
and the limestone to diopsidic and tremolitic
hornfels.
Organ Mountain batholith, New Mexico.—A
small discordant Tertiary batholith of about 55
square miles in area has been described by
Dunham (1935) from the Organ Mountains of
New Mexico, He infers that Tertiary andesite
flows form the roof for the intrusive comparable
with the roof of a laccolitli and that in depth
the body is crosscutting with steep outward
dips and was emplaced by piecemeal stoping.
There is evidence that some xenoliths have
sunk not less than 1400 feet and probably much
more. The dip of the andesite roof is away
from the batholith, exceeds 50°, and swings
around with the contact. Locally the wall rocks
have been powerfully distorted by magmatic
pressure. The batholith is composite and consists of three distinct bodies, a monzonite,
quartz monzonite and quartz-bearing monzonite. The quartz monzonite has tiny miarolitic
cavities as a widespread feature of a porphyritic fine-grained facies. The intrusive process
according to Dunham was accompanied by a
progressive concentration of volatile fluxes.
There are no pegmatites or aplites in the monzonite; aplites but no pegmatites in the quartz
monzonite (17.5 per cent normative quartz)
and aplites, pegmatites, and mineral veins in
the quartz-bearing monzonite (10 per cent
normative quartz). The aplites are very small
dikes and veinlets. Qua-ftz porphyry sills and
dikes occur in the country rock (Dunham,
1935, p. 84). Wollastonite (p. 100) has been
formed locally in the limestone contact with the
late intrusions.
Paleozoic leucogranite and granite porphyry
balholillis, Newfoundland.—Two examples of
Paleozoic miarolitic leucogranite or alaskite
batholiths emplaced in the epizone have been
described by White (1940) and by Van Alstine
(1948), both from the south coast of NRwfoiinrl-
land. The roofs of the batholiths are relatively hand it has a foliation throughout and is eiH:, The slates were changed to mica schists and to
flat, in part covered with roof pendants, and placed in dose-folded country rocks—char- injection schists, tlie quartzites to raica-garnetquartz rocks or to quartz-siliimanite rocks.
have gently outward dipping walls. The granite acters appropriate for the mesozone.
is miarolitic and homophanous. Chilled conExamples of plutons with transitional char- Local bodies of marble around tonalite have
lieen replaced by garnet, diopside, wollastonite,
tacts are rare but were observed. The St. Law- acteristics appear to be not uncommon
rence batholith (Van Alstine, 1948) of Devonian Europe. Several late Hercynian granite com-" idocrase, feldspar, etc. Many of the intrusive
(?) age has rdated rhyolite porphyry dikes in plexes in Portugal described by Westerveld bodies have zones next to their contacts that are
the country rock and epithermal fluorite de- (1955) are post-tectonic and almost wholly banded or gneissoid. Gabbro forms about 7
posits. It is elongated in a direction approxi- discordant, but also have steeply dipping per cent of the batholith, tonalite 63 per cent,
mately normal to the trend of the major folds planar foliation in substantial part parallel to granodiorite 28 per cent, and granite 2 per
and thrust faults of the Cambrian and Ordovi- the borders of the pluton, but locally at aa cent. Larsen is of the opinion that in the area
described the rocks had only a moderate temcian (?) rocks and is inferred by Van Alstine to angle.
perature when the first member, the San Marcos
have been emplaced by stoping. The Ackeley
•1
gabbro, was intruded, as small bodies of that
batholith (White, 1940, p. 969) is bdieved to
Sotdhern California Balholith
fock are rather fine-grained. Locally aplite
occupy more than 300 square miles. A
miarolitic alaskite facies is associated with
The huge batholith of Southern CalifomiJ dikes are miarolitic. Larsen does not discuss
molybdenite and muscovite metasomatism. displays predominant discordant contacts an! the possible depth at which the present level
Locally where the batholith is bordered by certain other features which ally it with pluton: of the Southern California batholith was embut states (1945,
volcanic rocks there is an agmatite zone 3 miles of the epizone, whereas the near absence of placed
.
. .p. .404). that it was
wide.
chill zones, and the occurrence of internaf probably intruded to within a few kilometers
Another discordant Devonian (?) batholith border foliation and local concordance of struc-Mo' the surface. Chayes (1956) is of the opinion
of the epizone has been described from the ture of country rock to contacts tie it to bath(>, liat the tonaiitic rocks are the product of a
mechanical mixture and interaction between
north coast of Newfoundland by Snclgrove . liths of the mesozone.
(1931, p. 24-25), Baird (1951, p. 49-52), and
The northern part of the batholith of South- granodioritic magma with previously solidiNeale (1957). The batholith occupies at least ern California has been described by Larsen fied gabbro. In most places contacts of the in75 square miles in area southwest of Confusion (1948), from whose work the following summary; 'trusive bodies are sharp. Chilled borders were
Bay, west of Notre Dame Bay. The rock is is made. The batholith is exposed for a length ,not found except in one granodiorite dike.
described as a granite porphyry or quartz por- of 350 miles and a width of about 60 miles, Il Merriam (1946) describes concordance of strucphyry. Foliation and lineation are marked in has a length of probably over 1000 miles if; ture of country rock with batholith contacts in
marginal facies. Many inclusions of Devonian discontinuous bociies at tlie southern end ait ,lhe Ramona quadrangle.
(?) rhyolitic volcanic rocks occur locally in the induded. The batholith was intruded in early
border facies. Neale (1957, p. 59) suggests that Late Cretaceous time. In the area studied by,
Balltolilh of Southwestern Nova Scotia
the volcanic rocks and the prophyry are in- Larsen the batholith was emplaced by more
The geology of the great batholith of southtimately related, and all the authors infer than 20 separate injections. The country rocb,
shallow intrusion. So large a batholith of granite were regionally dosely folded, metamorphosed,! Iwestem Nova Scotia (Fig. 8) has been sura- .
porphyry is very unusual, and it deserves addi- and intruded by eariier granitic rocks, perhaps Iraarized by Wright (1931). I t is more than 110
tional detailed study.
in late Paleozoic and Triassic sediments, the; [miles long, 20-30 miles wide, and together with
orientation of the inclusions and other strui^ [[satellitic bodies has an area of 4000 square
tures of the batholith, the elongation of the- imiles. The eastern part consists of biotite arid
PLUTONS OF TRANSITIONAL(?)
batholith, and the strike of the major faults ait] Fmuscovite granite that rardy shows gneissoid
EPIZONE-MESOZONE
in about the same direction. Larsen infers that, for banded structure. Aplitic and pegmatitic
tlie batholith was emplaced by stoping and not; [lades are common, and the texture of the granItUroduclion
by forceful injection. Forcing apart of the walb fite is maintained up to the contacts. The conThere are several batholiths whose descrip- may have been important in furnishing room; Itacts are sharp. Andalusite hornfels has locally
tion suggests characters appropriate in part for some of the elongate members of the bath; ibten formed in adjoining slate. The country
for the epizone and in part for the mesozone. olitli, but it could not have furnished a largt irocks are predominantly folded late PrecamThey are therefore here included in a transi- part of the space for the batholith as a wholt' Ibrian chloritic and carbonaceous slate and
tional (?) group until more definitive dassifica- He condudes that there is no relation between] [sandstone. The beds are in broad folds which
tion can be made. The Texas Creek granodiorite proximity to granitic bodies and degree of meta' jtre transected by the batholith, without apbatholith (Buddington, 1929a), a unit of the morphism, except for local contact metamorphl Jpreciable distortion or deflection. The invading
Coast Range intrusives of Southeastern Alaska, ism and for thin screens between intrusiw, Imagraa is inferred by Wright to have displaced
is representative of the kind of problem in- masses and small indusions. For the most parti |its host without appreciable lateral thrusting
volved. The batholith has a sharply discordant there is little contact metamorphism wherf Ror doming of the roof. Mesothermal gold-quartz
broad relatively flat roof, common aplite and the granitic rocks intrude large bodies of oldefj Kvems occur in the country rocks. Wright quotes
pegmatite dikes in the contact zones only, and schists, slates, and quartzites. Some of the] fiFairbault as estimating that 9 miles of the
assodated porphyritic aphanitic dikes. These screens and indusions in the granitic rockv {Precambrian Goldenville formation had been
=^u_^i.
;"""o-.On..t.he^other_ however, have been greatly metamorphosrf^ Eeroded, mostly before Mississippian time.
Locally the batliolith is reported to cut fossiliferous beds of Silurian and Devonian age. Most
of the data of Fairbairn (1957), however, based
on rubidium-strontium ages of mica suggest
ages of between 350 and 400 million years, or
between Middle and Late Ordovician. These
discrepancies in ages are at present unresolved.
The characters of the batholith seem to be
definitely those of the epizone, but it is-not
certain what significance is to be drawn from
Wright's reference to 9 miles of eroded material.
The axis of the batholith is in part strongly
discordant to the fold axes of the regional structure. The discordant Boulder-San Juan (Colorado) line of plutons, described cnriicr, mny be
referred to ns a much "ncnrer-surfnce" expression of similar relationship.
PLUTONS OF MESOZONE
"r/ie granite was once hot, ftdl of gas and
molten . . . if rose along a large broad front,
stretched out and expanded sideways and yielded
to a force from lite deplh which pushed and drove
il." Hans Cloos, 1953.
Inirodudion
It may be expected that a substantial period
of time would be necessary to permit erosion to
expose plutons of the mesozone. The fact that
no plutons of Tertiary age in North America
are known to the writer to be emplaced in the
mesozone is consistent with the foregoing principle. In the western Cordillera, Jurassic to
Lower Cretaceous plutons, however, are dominantly of mesozonal character.
Cliaracteristics
The individual plutons of the mesozone are
inferred normally to have the following characteristics. The degree of metamorphism of the
regional country rock is not more intense than
the green-schist and epidote-amphibolite facies.
The argillaceous country rodcs of sedimentary
origin are usually slates and phyllites. The inferred temperature of the country rock at the
time of intrusion is generally no higher than
400°-500''C. There is no apparent direct rela. tionship between the plutons and volcanic
rocks. The stocks and batholiths are effectively
always of composite character made up of two
or more units. The units in general vary systematically; the younger intrusions are more alkalic and siliceous. The characteristic plutons
have complex emplacement relationshios to the
i a ^ u i ^ y i - . j \js: i j v / u v o i i i u i - V A U V r ; Jii-lAUMIi-JVlE-SUiiUWi:,
country rock—in part discordant, in pari concordant. Locally there may be some replacement; Some may show transection of roof in
ally, gentle dips in the core or parts of thei
may indicate a domal roof. The planar struct
of some plutons may suggest a rough fun
S«ctlon etonA line B-A., modlOed a f t a r
C,R.raribault,(>ological Sjrv^ Canada,Map UA
FIGURE 8.—GREAT DISCORDANT DEVONIAN (?) GRANITE BATHOUTH OF SOUTHWEST NOVA SCOTU J
core of the pluton without planar structure,
limilation may be significant in border or
zones. Wall rocks in the contact zones often
the development of a steep schistosity
iormable with the contact and with a linear
cture more or less parallel to the dip, inting flowage in a subvertical direction,
lift of Uie roof rriay be inferred. Minor fold
' and lineation of country rock adjacent to
t"pluton may have steeper plunges tlian fur' away (Trefethcn, 1944, Pl. 1). Bedded
or dikes at large angles, to the contact
iy be crumpled back on themselves as though
formed by outward pressure from the pluton.
ded rocks or older sills parallel to the conmay show boundinage structure due to distion.
Emplacement by reconstitution and replacet of country rock is commonly either absent
subordinate. An occasional small pluton,
wever, may be emplaced wholly by replacet. Chill-border facies, in the sense of aphac texture, are absent. Typical migmatites
commonly minor and are often absent. Pegtites and aplites, however, may be common,
specially in border zones. They may have a
Idial fabric in some plutons. Miarolitic struc!re is absent. Marginal fissures with inward
ips, in part lined with aplite or pegmatite,
lay be present locally in border zones of plums. The plutons are pre-eminently those where
ie applicability of Cloos' system of "granite
Ktonics" is most rewarding,
'Some batholiths may be bordered by a zone
I dike injection or contact agniatites. Dikes
"ig. 13) or dike systems (PI. 1) as well as sills
By occur in the country rocks bordering the
!trusives. Hutchinson (1955) has shown that
ithe Ross Lake area. Northwest Territories,
inada, pegmatite veins of an area of several
'
,.
.,
T
^i.
i_ ^^
.,
^\.
E- 1 J • 1
.. r •
\ /i\ c
*/. .,7 T ,,r • L /,n-,< .j-u nnodioritc. In the hottest zone near the granEmplaced in lower part of epizone or upper part (?) of mesozone. After W. T. Wright (1931, modiBB
,. i
j
i j u
after E. R. Fairbault)
KF p
v/
• " » " - •
|- Ithey are often large and emplaced by gran'f. Ization of granodiorite layers whereas in a
ids along dilatant fracture zones, in part
the axis
or atupmoderate
archlike shape, and have steep outward flaring with
structure
eithervertical
right side
or upsideindinii
do* * ' " ^""^ ^ h ^ were emplaced as pegmatitic
tions;
often
the
structure
may
be
as
shown
iJ
l
\ ^ ^ ^ development of zoning of the "cornwalls in depth. Rardy, a mass such as the Sugar
Figure
9.
Younger
units
may
crosscut
the
folii*^
^i^P^ of Pegmatite
Hill pluton in Vermont (Doll, 1951, p, 44) has
Contact-metamorphic aureoles may be well
crowded a series of uniformly north-northeast rion of older units, or locally the planar flp»' eloped around stocks (Philbrick) 1936;
trending metasedirnents into a conformable structure riiay be independent of boundariesd tcher and Sinha, 1958) and small batholiths
steep- dipping funnel. Planar foliation is often units within a composite pluton (Fig, 9) ani | d around areas of dike comislexes in roof
well developed, cspedally in the outer portions maintain its swing across their contacts,
'ines (Eric and Dennis, 1958, PI. 1). In the
of the pluton, but commonly is local, elusive, planar structure in some plutons is iri part
•ger or relatively deep mesozonal batholiths
tematicftlly
oriented
at
an
angle
to
the
oul
or.missing in the core. The planar structure of
border of the oluton. Linear .qtrnrtiirp. rail jonal metamorphism is associated. Phyllites
canic rocks or metalimestones in the vicinity of
contacts. A schistose structure is common in the
country rock bordering mesozonal plutons.
Mesozoic Plutons wilh Both Discordant
and Concordant Relations
to Country Rock
While Creek balltolilh, British Columbia.—A
late Mesozoic batholith described by Reesor
(1954), from British Columbia shows deariy
many significant phenomena (Fig. 9). The
country rock consists of the Proterozoic Lower
Purcell series regionally recrystallized to phyllites, little deformed in the eastern part of the
area but compressed into isodinal folds in the
western part. The rocks belong to the greenschist metamorphic facies. The batholith is
about 12 to 17 miles in diameter. There is a
contact-metamorphic aureole of about 1000
feet diameter, and all the rocks of the contact
zone are schistose. The batholith crosscuts a
north-plunging antidine of Proterozoic rocks.
Although the batholith in part truncates preexisting structures, the bordering strata are
generally visibly and -violently side-thrust and
forced to conform with the direction of the contact. Vertical isoclinal folds occur along the
north and south borders. In one area a marked
cross deavage has developed; fracture deavage
has developed in competent beds, crenulations
with deavage paralld to axial plane in phyllites,
and a planar foliation across the bedding. A
vertical upward motion of the magma during
emplacement is indicated by the. vertical to
near-vertical lineation and by joints. Evidence
of stoping is indicated by an almost universal
irregularity of the contact of the pluton with
country rock and by local stoping. Inclusions
occur everywhere in varying amounts, except
within the interior granite. The rocks of the
batliolitli consist, in order of their emplacement, of biotite granodiorite, hornblende granodiorite, and porphyritic granodiorite in
roughly concentric arrangement with an elongate core of quartz monzonite. The quartz
monzonite grades into an aplitic facies which
cuts the other rocks. Aplites and pegmatites
occur in great abundance in parts of the mass,
notably in the porphyritic granodiorite but not
in the quartz monzonite. Inward-dipping
joints are well developed throughout the batholith, and many are filled with aplite or pegmatite. They rarely extend into the sedimpnt<;
698
699
PLUTONS OF MESOZONE
A. F. BUDDINGTON—GRANITE EMPLACEMENT
EXPLANATION
IGNEOUS
ROCKS
Lote Mesoioic
i 0 « c f l l monioo'te (Ofn)
o,d
tpn\ Aplillc gronodiorile <0Qdl
pgd
PwphfiHlc qroiwitofite
1 HornWende ^^'^'* I trioi^lB qronwliorilft
bqd
qf
Biotite gronodiorile
GronitB
SEDIMENTARY ROCKS
Proleroioic
Ouoriiile, orgiltilt,
(WffT^iHc quottille ond
dolomile; repfMtnloUve
rormoron boundories
oytlifwd.
Outer contoci ot
- ^
^
bolhoimi
Veflicol fofiotion
Slrltt ond dip ol
^
(oliolion
SIriha ond dip o>
^
bedding
/
FIGURE 9.—^REPRESENTAHVB <
fK BATHOUTH OP MESOZONE
\
,
^
„
„nc.i\
In part discordant, in part concordant because of crowding aside of count Kreek batholith, British Columbia. Modified after J. E. Reesor (1954)
inferred to have originated at the last stage in
• consolidation of the interior granite. The interior planar foliation is universally vertical to
jubvertical, and although generally conforra•
C-lU^
_Kai.Kf\lith_it_locally_
locally at the border contact of the complex it
follows every irregularity. There is no linearl
structure in the quartz monzonite. A mafic-riiij
fades of the granodiorite may be due to i
poi^tipn as indicated by the presence of
I Sierra Nevada batliolith, California.—The
(Sierra Nevada pluton is about 300 miles long
land 50-60 miles wide. I t has not been fully ex.plored, and an adequate systematic unified
[description of the existing data is not available.
the Yosemite area, and Cloos (1936) has published a structural study of the batholith of
Yosemite National Park and vicinity and of an
area northwest of Lake Tahoe. The structural
study has been effectively summarized by Balk
^10-^7
i-i
fi^—A7^
Onlv
Qfin-ip
nprtinPnh
irfpac
from literature later than that available to
Balk will be cite,d here.
Hamilton (1956, p. 21-23) has given a summary upon which the following abstract is
based: The granites were intruded in hundreds
of separate plutons, some a few acres in extent
and some covering several hundred square
miles. Contacts are sharp, and gradation from
granite to country rock commonly takes place
in less than an inch. The uniformity of the granitic rocks over wide areas, and the gradual
nature of the variations indicate that large
volumes of the material could be mixed and
homogenized. Some of the intrusive material
seems to have been wholly liquid (as in the
alaskites), whereas some was only partly liquid.
The granites intruded and produced contact
metamorpTiism of a country rock which had
already undergone moderate regional metamorphism. Structures in the metamorphic rocks
are cut across sharply by the granites, and
straight dilation dikes from the granites transect contorted metamorphic rocks. I t is possible, however, that some of the deformation of
„ • the country rocks was the result of forces of
intrusion acting before establishment of the
final contacts. Early plutons intruded the metamorphic rocks; later plutons intruded earlier
plutons.
The intrusive granites moved generally upward, as shown by .their flow structures.
Hamilton states that stoping operated, but to
a degree that is only conjectural. He infers that
an explanation in terms of cauldron subsidencesloping on a huge scale could account for the
. eniplacement of some of the plutons, particularly the smaller ones which are intrusive entirely into other plutons. However, he finds
that no evidence for such emplacement has
been recognized in the Sierra except that the
geometry of some contacts might favor it. His
condusion is that the plutons formed from mobile magmas which moved upward and expanded outward, mostly passively but in part
fordbly. Large amounts of material were incorporated into the margins by assimilation of
_ wall rock and stoped blocks, but most of the
granitic material was introduced from I lower
levels.
Durrell (1940), Macdonald (1941), and Mayo
•(1941), who have studied contact rdations in
the Sierra; have conduded that, whatever the
rtieans of intrusion, these means were passive.
• They find that contacts are mostly complexly
discordant in detail and, if the wall rocks were
^shouldered aside, it was apparently accom-
I-
zones about the intrusions, not witli shearing
along the contacts.
Mayo (1941, p. 1081) suggested that th
dominant means of emplacement of Sierra
plutons was "permissive intrusion, tectonically
controlled," and "the structural features of thei
region seem in harmony with the idea that spaey
for the intrusion was provided . . . mosdy b «
buckling of the isodinally folded wall rocks ay
a result of a north-south compression".
Durrell (1940) and Macdonald (1941) be
lieve tliat the belts of country rocks within the
batholith are roof pendants with relativeij
flat bases, remaining portions of a once-con^
tinuous roof. They agree that the contacts of
the igneous bodies dip outward in most places
60°-70° and that there is a suggestion that the
upper parts of the stocks, and probably all the
larger intrusives, are more or less dome-shaped.
Balk (1937, p. 67), on tlie basis of the work of
Cloos, states that an eastern pluton of the
batholith in the Yosemite region has what
might be called a schlieren dome were it not foi
a small mass of structureless granite at the corej
and that "each schlieren dome, or arch, is com;
posed of a number of dosely related, but petro
graphically different, rock types which tend to
conform with the dome structure, as a system of
concentric shells". This pluton also shows marginal upthrusts along the contacts of the oldest
intrusion. A comparison of the geologic map by
Calkins (1930) and the structure map of Cloos
suggests that the flow structure in part crosses
the boundary of units as in the White Creek
batholith, British Columbia. The foregoing discussion deals largely with the central part of
the batholith. Webb (1938, p, 315) finds that in
the southern more deeply eroded part of the
batholith the foliation of the septae have highj
angle dips, none less than 60°-.
Coasl Range balholith, Alaska-British Cahm
bia.—The upper Jurassic to Lower Cretaceous
Coast Range batholith of Alaska and British
Columbia has a length of at least 1250 miles
with widths of 35 to 60 miles common and up t(
a maximum of 125 miles, A substantial part ol
the batholith consists of screens of schist and
gneiss. There are few detailed maps of any part!
of the batholith.
The batholith in a general way parallels the
trend of the prebatholithic structures, but only
in a general way. Phemistcr (1945, p. 79) notes
that near Vancouver, British Columbia, "The
country rocks strike slightly north of east, while
the batholith has its greatest extension froni
south to north". Buddington (1929, D, 29J
J^olith as extending for many miles parallel to
II the strike of the adjacent formations, although
locally crosscutting; he notes that for a length
of 40 miles the batholitliic margin strikes neariy
north and transects the general structure at an
angle of 15° to 40° whereas the northern part
trends northwest at a slightly greater angle
than the formations of the country rock. The
batholith is stated to work across a syndinorium of Mesozoic rocks into Carboniferous rocks.
Smith and Stevenson (1955, p. 816-817) write
iconcerning the emplacement of the intrusives
j|in southern British Columbia that in many
•J places the batholiths transect the structures of
\i the country rock, that in some places much of
the rock was pushed aside, and that trend lines
around tlie southern end of the Coasi: Range
batholith were probably formed by broad-scale
4and strong lateral pressures transmitted
I through the magma. The formations southwest
<of the batholith in southeastern Alaska are
^generally isodinally overturned to the south^ west, and their dip and the dip of the foliation
:•* of the border belt of the batholith is steep northl east or verrical.
* Also in southeastern Alaska (Buddington,
• 1929, p, 181) reconnaissance indicates that the
quartz diorite is predominant in the south,• western part (5 to IS miles wide) of the bath_ olith, and quartz monzonite is predominant in
the eastern part (10-15 miles wide) with mixed
.rocks of generally granodioritic character in
.'the core. Smith and Stevenson (1955, p. 811)
'describe the igneous intrusions in southern
« British Columbia as consisting of dioritic to
; granodioritic rocks in the western portion on
Vancouver Island, predominantly granodiorite
in the Coast Range, and principally granitic in
central and eastern British Columbia. The foregoing relationships recall the Sierra Nevada
batholith about whidi Durrdl (1940, p. 12-13)
I writes that by far the most abundant plutonic
•i rock in the area studied by him (southwestern
[• part of batholith) is quartz diorite but that the
I most easterly plutonic rocks are quartz monI zonite and granite, and that there is a gradual,
I although overlapping, progression from basic
It types in the west to acid types in'the east.
^i The batholith is exposed along Tracy Arm
in southeastern Alaska for a width of about 15
•k miles at an angle of 60° to the trend of the
Ip major structure. The intrusive rocks contain
many large belts of injection gneiss and so many
inclusions of country rock that it is doubtful if
any area as much as 10 feet square is clear of
them (Buddington, 1929, p. 69).
I
I
part of the Coast Range batholith in southeastern Alaska have characteristics definitely
like those of bodies emplaced in the mesozone;
the southwestern part of the main batholith
and the adjoining country rock equally definitely have characters like those of the
catazone. The northeastern part of the batholith appears to belong to the upper part of the
mesozone or even the lower part of the epizone.
A difference in degree of metamorphism of the
country rock bordering the western and eastern
parts of the batholith was early recognized by
the Wright brothers (Wright, F. E. and C. W.,
1908, p. 67) and discussed later by Schofield
(tH Schofield and Hanson, 1922, p. 65-66) and
by Buddington (1928, p. 293-294). The batholith in southeastern Alaska is bordered on the
southwest by a belt of medium- to high-grade
metamorphic rocks. This belt has a width of
about 35 miles at the southern border of Alaska;
it narrows and pinches out at the north near
Juneau. The belt of metamorphic rocks changes
in metamorphic intensity toward the batholith
from the general regional green-schist facies on
the southwest through garnet-biotite and staurolite-kyanite zones to a sillimanitic facies with
a migmatite zone adjacent to the batholith.
There are many plutons of granodiorite or
quartz diorite throughout. The rocks to the
northwest along the southwest border of the
batholith and along the northeast border of
the batholith are slates and greenstones. It
might be suggested that the belt of medium- to
high-grade metamorphic rocks on the southwest border overlies an extension of the main
batholith at depth and that the overlying schists
were forced up from deeper zones by the upward push of underlying magma and by the
accentuated upward drag of the magma mass
which formed the southwestern part of the
main batholith. The mechanism suggested resembles, but on a larger scale, the idea of upward drag or upward thrust of walls by rising
magma proposed by Noble, Harder, and
Slaughter (1949, Fig. 4). The quartz monzonite
and granitic rocks of the eastern part of the
batholith are younger than the quartz diorite
of the western part. Granodiorite porphyry
dikes of a character appropriate for the epizone
are abundant locally in the country rock of the
eastern border and are inferred to be related to
the quartz monzonite.
Mesozoic Pseudo-igneous Pltdons
or Facies of Mesozone
Swedes Flat plidon, California.—Two ex-
vjAxfvt-iXXi:* i^iyi.ri.jr\\.,M:.lviLjLy X
as emplaced by recrystallization and replacement in the mesozone are the Swedes Flat stock
in California and the Chilliwack batholith in
Washington. The roof (Pellisier granite) of the
Inyo batholith, California, has also been interpreted as a product of recrystallization and
replacement.
Compton (1955) has described the Swedes
Flat pluton and interpreted it as the product of
recrystallization and replacement. The main
mass of the pluton is about 5 by 7.5 miles in
diameter. Tonalite and granodiorite form the
preponderant bulk of the pluton with about 4
square mUes of gabbroic and dioritic rocks at
the north end and another mass at the soutli
end. Granophyre forms a local late intrusive
phase. Gradational contacts between granodiorite and dark hornfds and amphibolite are
striking. The latter give way to homogeneous
granodiorite through a broad zone of intricately
veined mixed rocks, 100-1000 feet wide against
gabbro and diorite, up to 3 miles wide against
metavolcanic rocks. The regular, gradational
changes from the incipient webbing of these
mixed rocks to indusion-charged granitic rocks
and then to granitic rocks with only vague hornblende dqts suggest that tlie granitic rocks
have passed through these stages in their development, Compton believes that a replacement origin for the homogeneous rocks is supported by their lack of flow structures or fracture pattern and by the fact that the foliate
indusions fit the projection of country-rock
foliation through the pluton rather than any
reasonable - movement picture within it. He
suggests, that most of Uie granitization was
produced by fluids moving in open channels
and that the source of these fluids was probably
a magma that formed the core of Swedes Flat
pluton. Such a magma he infers would have
lain south of, and perhaps at a lower level than,
the rocks as now exposed.
Pellisier granite facies of Inyo balholith, California.—The Pellisier granite facies of the Inyo
batholith, California, of middle or late Mesozoic age has been interpreted by Anderson
(1937) as a roof facies of a major batholith developed in situ by replacement and recrystallization of both sedimentary and igneous
rocks. The granite carries abundant indusions,
most of which appear to have originally been
schistose or argillaceous. The replacement
origin he bases upon field evidence of gradation
between country rock and granite, the variability in composition of the granite, the inherit'-"-"'""•-tiire.dosdy.r.esemblingstratifica-
rjUUXUINS U f
replacements, espedally albitizatibn. The paJi
int after much of the complex is solid. The
of the batholith mapped is 35 miles long, T l ' | allowing summary has been made from the
Pellisier granite is in substantial part a hon
•scriptions by Waters and Krauskopf (1941)
blendic granite, whereas the main part of th
(d by Poole (1956).
batholith is a biotite granite. The solutions^
The Colville batholith intrudes folded and
effecting the development of the Pellisier granite, dynamically metamorphosed sedimentary and
are inferred by Anderson to have been derived Volcanic rocks of late Paleozoic and Triassic
from the underlying magma which crystallized ,»ge. The age of the batholith is thought to be
to form the main part of the batholith. Migmat' tite Jurassic or early Cretaceous. I t is about
miles long. Waters and Krauskopf describe
titic gneisses have been formed in the bordelj
rocks of the batholith at depth.
'j he batholith as remarkably heterogeneous
Chilliwack balholith, Washington.—The de- both structurally and petrographically. A censcription by Misch (1952) of-the Chilliwack tral mass of structureless granodiorites grades
batholith, Washington, affords an example in outward into a belt of foliated igneous rock
which the hypothesis of granitization has been ^which commonly shows intricate swirling of
applied to explain the development of a batho-lj he foliation. These swiried rocks grade into a
lith in the mesozone in the latter part of theli 'iieripheral belt of variable but well-foliated
Mesozoic, The batholith is about 35 miles long imigmatitic gneisses characterized by severe
and 5-10 miles wide in Washington and ex- granulation of the constituent minerals. Over
tends north into British Columbia. The country broad zones they find that this rock is a mylorocks are a series of geosyndinal rocks, mostly nite and that locally recrystallization has prophyllites, quartzites, marbles, greenstones,, duced types resembling metamorphic granuand greenschists except at the southern end of^ lites. The trend of the folds (in the country
the batholitli where, in the border zone of the rock) as well as the direction of foliation and
batholith, the phyllites are changed to mica other structural features is predominantly
schist, and the greenstones and green schists northwest-southeast, .and across these structo amphibolites. The granodiorite and quartz tural trends the batholithic border cuts with
diorite of the batliolith are inferred by Misch decided discordance. The wall rocks a t the
to be the result of a continued granitization periphery of the Colville batholith show almost
process which first yields a series of granitic no evidence of contact metamorphism. Peggneisses (the Skagit gneiss) and then large di- matites are abundant near the border.- From
rectionless granite bodies with gradual passages-! idetailed consideration of rdations both within
between. The country rocks on this hypothesis . ,the wall rock and within the adjacent intrusion,
are not pushed aside along part of the contact,*, however. Waters and Krauskopf suggest that
but in part the granodiorite is reported to have the features of the contact zone can best be
moved as a plastic crystalline mass and intruded * attributed to the rise and emplacement of the
the metamorphic rocks. Several smaller bodies I batholith as a unit. By this interpretation they
appear as isolated intrusive stocks which have i infer that the intense brecciation and usual
forced their way by pushing the metamorphic ; lack of metamorphism in the wall rocks is due
rocks aside. Part of these intrusives are in Lower to a rise of the intrusive at a time when its
Cretaceous rocks. The magma of these intru- peripheral portion (which now forms the gneissions is assumed by Misch to have formed at: sicand mylonitic facies) was nearly solid. Where
depths bdow the level now exposed as the final.- the linear structure-shown by swirl axes is well
dimax in a long process of granitization andi ideveloped, the prevailing pitch of the axes is
mobilization, and it is stated that it did not: iinvariably northwest. They take this to indicate
come.from far away or an unknown depth. The' .at least a slight regional control of this strucdepth of formation of the granitic gneisses and- J ture. The core of the intrusive mass is hogranites he estimates at three or four to ten mophanous and composed of granodiorite and
quartz diorite.
miles.
The following description and interpretation
of certain phenomena shown by the Cassiar
Mesozoic Pltdons with Protoclastic or Latejj batholith is taken (rom Poole (1956). The bathStage Poslcoiisolidalion Deformation
;Olith is of late Jurassic or Early Cretaceous age
Colville, Washington, and Cassiar, British and is 13 miles wide by 70 miles long. The
Columbia, balholillis.—The Colville and Cassiar M'country rocks are sedimentary and volcanic
batholiths are discussed together as they both rocks regionally folded and metamorphosed in
•" ' *—'•'•--"«="lf«.of_continu5djiiagma move- .the greenschist facies or of lower metamorphic
MJibUiiUINJi
/UO
grade. The Cassiar batholith is largely a biotite granodiorite and quartz monzonite. The
western part of the batholith for a width of
about 4 miles is a strongly foliated catadastic
gneiss, whereas the interior and the eastern
part is effectively massive though foliated in
places. The central and eastern part is relatively undeformed. There is evidence for shouldering aside and uplift during the emplacement of the magma although it is unlikely that
all the space occupied by the batholith was
made in this manner. Poole infers that the
cause of the deformation of the western border
zone was renewal of intrusion in the solid state
such that the northeast part of the batholith
and adjoining sedimentary rocks moved up
and perhaps southwest relative to the southwest border zone, producing the northeast dip
of the foliation. He notes that the sedimentary
rocks for several miles southwest of the
batholith are in isodinal folds with a southwest dip, and it is unlikely that this would have
persisted if regional deformation had acted- to
produce the northeast-dipping foliation of the
west part of the batholith.
Precambriati Batholitlis of Mesozone
General statement.—It has been noted that
stocks emplaced in the epizone may be of
Precambrian age, and so also may Precambrian
stocks and batholiths belong to the mesozone.
The Giants range (Allison, 1925) and the
Vermillion (Grout, 1925) batholiths in Minnesota may be examples, and descriptions of
others follow.
Noranda-Senneterre belt, Quebec.—Several
batholiths of granite and granodiorite occur
as intrusives in a series of intermediate and
basic flows with subordinate tuffs of the Keewatin series and Timiskaming sediments in
the Noranda-Senneterre belt, Quebec. The
country rocks have complex structure and a
low-grade regional metamorphism. Norman
(1945) and Tremblay (1950) have described
some of these batholiths, and .a map and
description of structure on which Figure 10 is
based have been published by Dawson (1954).
The batholithic rocks indude muscovite
and muscovite-biotite granites and homblendic varieties; the homblendic varieties
are quartz poor.
- The boundary of the La Motte batholith
is almost wholly conformable with the foliation of the country rock but does transgress a
series of metasedimentary beds at one locality.
The foliation indicates an elongate domal roof
with moderately dipping walls on the north
and steeply dipping borders around the rest
of the pluton, Migmatization occurs very
locally. Pegmatite forms nearly SO per cent
of the rock in a zone half a mile to a mile wide
around the border of the pluton and at least
10 per cent of the interior of the pluton.
The Lacorne batholith has borders which
are essentially concordant on the north and
south but which on the east cut directly across
the strike of the enclosing formations, Migmatization occurs locally near the southwest
border of .the pluton. Certain large inclusions
have been moved from the vicinity of the walls
and rotated. Thin lenses and dikes of granitic
material have been injected in peripheral
metasedimentary rocks. The foliation of the
pluton indicates a structural dome in the
northeast part of the main mass and another
in the southwest part. As in the La Motte
pluton the north border dips moderately, and
the south border steeply. Dawson infers that
the Lacorne pluton originally had steeply
dipping walls and may have been slightly
overturned toward the southwest.
The satellitic intrusions are interpreted as
unroofed cupolas that join the main granite
mass at depth.
Dawson (1958, p. 232) on the basis of a multivariate variance analysis of the mineralogical
compositions concluded that the batholiths are
composed essentially of a quartz monzonite
that is homogeneous within the individual
massifs and also within the intrusives as a
whole.
The intrusions are all interpreted by the
authors as of magmatic origin. The age determination (Shillibcer and Cuming, 1956) of
mica from the Lacorne pluton by the K^'-A""
method gave 2500 ± 150 m.y.
Pltdons north of Great Slave Lake, Northwest
Territories.—Batholithic emplacement in Precambrian rocks north of Yellowknife on Great
Slave Lake, Northwest Territories, Canada,
has been described by Henderson (1943) and
Jolliffc (1944), and Uie following is an abstract
of their work. The country rocks away from
the intrusions (Fig. 11) consist of graywacke,
slate, and volcanic rocks. Pillowed lavas are
so little metamorphosed that tops of flows can
be determined. Clilorite and seriate are common in tlie graywacke and slate. The rocks are
isodinally folded with steep dips. Henderson
bdieves that the isoclinal folds in turn have
been warped into syndinal- and antidinal-like
structures with the axes of the secondary folds
plunging neariy vertically. The granitic batho-
liths of granodiorite and quartz diorite were
emplaced in the refolded isodinal rocks with
accompanying metamorphism of the formations in the vicinity into andalusite cordierite
and quartz-mica schists (locally with staurolite)
and hornfels. The outer boundary of metamorphism crosses the trends of the folds. The
granitic batholiths are concordant, and Henderson infers that lateral pressures of invading
magma may have produced deformation. The
sediments and volcanic rocks dip away from
the batholiths at steep angles. There is a series
of small younger muscovite-biotite granite
stocks that have also produced similar metamorphism of the country rocks. Many granite
pegmatite veins are discordant with the foliation of the country rocks.
' I.
Supplementary Descriptions of Plutotis Emplaced
in Mesozone
Inlrodttction.—OtheT excellent detailed descriptions of mesozonal plutons in the western
Cordillera are those by Taubeneck (1957) of
tlie Bald Mountain batholith in Oregon, by
Smith (1947) of the Surf Point stock.in British
Columbia, by Krauskopf (1943) of the Wallowa
batholith in Washington; and by Compton
(1955) of the Bald Rock batholith in California. Plutons emplaced in the mesozone are
also dominant in most otlier orogens, but descriptions of only the Snowbank stock in Minnesota and the Enchanted Rock batholitli in
Texas will be referred to here.
Bald Rock batliolith, California.—The Bald
Rock batholith, California, described in detail by Compton (1955), shows many characteristic phenomena of the mesozonal batholiths.
The Bald Rock batholith is one of four plutons
in a chain somewhat more than 40 miles long
of small satdlitic intrusions that lies 20 miles
west of the main Sierra Nevada batholith. The
batholith is about 9.5 miles wide, a little more
than II miles long, and has an area of about
80 square mDes. The bedding of the country
rocks swings concordantly around the balholith, and Compton interprets it as formed by
a forceful intrusion. However, he also notes
that local crosscutting relations show that
about a fourth of its area at the exposed level
was gained by other means, and that large
concentric outliers and a hull of injection
migmatite suggest stoping. Indusions arc
scarce, but gradational zoning of the batholith
from a trondhjemite core through granodiorite
to a heterogeneous tonalite rim suggests that
,1 u
rj
I ,
r
i
i jL*u x v / i \ o v/i" lYiJuoKji^yjiyiZf
liasic stoped rock contaminated an originally
Irondhjemitic magma.
Contact-metamorphic rocks of epidote amGranitic inirusivts
phibolite to possible pyroxene hornfds form
jpjT^Xhottaa fuar~ei-/nica schigt
•n aureole that has an area nearly as great
F.'M-'i-J rxnti AornAsCs-<iai~ixtai£/rom
B the original kinetic intrusion. Squeezing
firx^wa-cAa, sCate, ate,
«nd verrical stretching of wall rocks is indicated
SrejruxLcAa, siaie, imjourv
V pebbles of conglomerates and crystal line•
aniost aneC ^uartxiea
>lion, most pronounced near the contact.
Volcanic rocAs.
The zone of the contact migmatites is only
> few feet to a few tens of feet wide where
Muntry-rock foliation is parallel to the contact; but it is as much as a quarter of a mile
wde where the contact is sharply discordant
to foliation. Most of the granitic parts of the
contact migmatites occur as sharply bordered
dikes that generally parallel foliation but
[locally cross it. The flow structure of the intrusives is more obvious near the contact be|cause mafic minerals and indusions are here
|inost abundant, but its actual perfection,
grain to grain, does not vary greatly from the
nm to the core of the intrusion. In some places
die flow surfaces parallel the gradational
boundaries between rock types, in other cases
Ihey cut across them at large angles. There
.ire several extensive, unconformable junctions
i the flow lines that are probably local intnisive contacts. Notably, the flow structures
ip as steeply at the core as any^vhere in the
trusion. In the west half of the pluton tliere
e thousands of thin aplite and pegmatite
'iiikes, in the east half several large dikes and
:pipes of aplite and microgranitic rocks. Almost
ill the dikes are vertical and trend at about
ight angles to the flow .structure. Thus they
Ilan out on the flanks of the trondhjemite mass.
The late-emplaccd bodies in both halves of
the batholith are interpreted as controlled by
ladial fractures resulting from upward pressure
W an underlying mobile core. The way in which
the flow layers locally cut across the gradajtional rock boundaries poses a considerable
problem. Compton's suggestion is that im_mobile tonalite -was forming near the contact
iivhile granodiorite was forming somewhat
[farther from the contact, and in some cases
iKhile trondhjemite 'was forming still further
Irom the contact. He believes the flow structures
uid their overall pattern can be explained only
by assuming that the magma was mobile during the growth of the batholith and that grain
jsrientation took place when a zone of mobility
slowly grew into the intrusion from its walls.
FiGiTRE 11.—PRECAMBRIAN BATKOUTHS EMPIACED IN MESOZONE
_ Larsen and Poldervaart (1957) state that
^ote discordant boundary of zone of metamorphism; from Henderson (1943) reproduced bv courtesyl
he Amencan Journal of Science
'
' I' "The distribution of two distinct zircon popula3ns in the Bald Rock batholith as well as strucVEGBND
tural relations demonstrated by Compton, are explained in terms of a parautochthonous intrusive of
migma-magma, with solid phases predominant at
the borders of the pluton and silicate melt predominant in the core".
Larsen and Poldervaait emphasize that
xenoliths are concentrated between the trondhjemite core and granodiorite-tonalite rim but
are rare in the rim itsdf.
The Merrimac pluton to the north, described
by Hietanen (1951), shows many similar
phenomena.
Snowbank slock, Minnesota.—The Precambrian Snowbank stock, Minnesota, described
by Balk and Grout (1934) is a very fine example
of a typical stock emplaced in the mesozone.
I t is an elliprical mass, 3 miles wide by 5 miles
long, with planar foliarion in the borders and
a faint linear structure throughout, although
a late granite portion is almost massive. The
country rocks are strongly crowded outward
with structures largely conformable with the
contact, and tlie magma rose steeply as a
cylindrical mass at an angle of about 70°.
Enchanted Rock balholith, Texas.—A pluton
emplaced in quartzo-fddspathic gneisses and
high-grade metamorphic schists has been described by Hutchinson (1956) as the Enchanted
Rock batholith from the Precambrian of Texas.
Although of Precambrian age and intruded in
high-grade metamorphic rocks, the batholith
has some characters of those emplaced in the
mesozone. It is also exceptionally interesting
in that one-third of the batholith has a phacolithic relationship to the country rock. The
batholith is 9 miles wide and 15 miles long.
The batholith shows predominantly a peripheral concordance of the country rock with
the border of the pluton, with minor discordance. Except for the phacolithic part of
the batholith the foliation is nearly vertical
throughout. The lineation is also nearly vertical, and during the early stages of intrusion
and crystallization the principal direction of
transport is inferred to have been vertical.
Marginal fissures are restricted to the outer
mUe-'wide perimeter, dip 10°-25° inward, and
are filled with pegmatite and aplite. There
is one joint system with steep dip, subradial
and at right angles to the planar structure,
also filled with pegmatite and aplite. Chilled
border rocks are 10 to 2 feet wide. Hiatal porphyritic texture prevails in chilled borders
and apophyses. The phacolithic part occupies
a syndinal trough plunging 35°-40°. There are
four concentric zones of different granitic
facies within the pluton.
'\l
PLUTONS OF TRANSlllUINAJj ivi£.auz,uiNJ:--t-rti/vt.ui^i
Hutchinson infers that the batholith was
emplaced at a late stage in the deformation by
forceful injection and that not more than 5
per cent of the batholith is of replacement
origin. The age given by the "Larsen" method
is 815 m.y.
PLUTONS OF TRANSITIONAL
MESOZONE-CATAZONE
General Discussion
In a number of regions part of the plutons
have characteristics of the mesozone, and part
those of the catazone, although both are of
similar age. Individual plutons also have some
characteristics of both the mesozone and the
catazone. Such mixed associations or. diaracteristics appear to occur particularly in plutons
emplaced in rocks with an intermediate grade
of metamorphism; that of the epidote-amphibolite or staurolite-kyanite subfacies. Where
plutons are of similar age in the same region,
yet vary from mesozonal to, catazonal, it seems
probable that we are dealing with local variations in the physical conditions at the site of
emplacement rather than with different depth
zones. In many such examples the pluton with
characteristic of the catazone may be the roof
facies of a mesozonal batholith,
Plutons of Wolverine Complex, British Columbia
Armstrong (1949) describes the Wolverine
complex as occupying more than 1000 square
. miles in Brirish Columbia. According to him it
indudes a series of micaceous quartz-feldspar
gneisses (in part with 40 to 65 per cent quartz)
and migmatites with'granodiorite plutons (up
to 10 square miles) formed in place by progressive injection of granitic material and gradual
replacement of injected rock. Roots (1954)
considers the complex was formed by a metamorphism and granitizarion superimposed on
previously regionally metamorphosed Proterozoic and Lower Cambrian sedimentary beds
whose grade of regional metamorphism increases in intensity with successively lower
stratigraphic horizons, low-grade quartz-chlorite schists; crystalline limestone, slate, phyllite, chloritoid schist, and graywadies in
the upper part of series; quartz-mica schists,
quartzite, garnetiferous schists, and kyanite
and staurolite schists in the lower part of
series. The regional metamorphism he bdieves
preceded folding, and the temperature rise
-»..«-WM»j„,na.r.i:_to_emDlacement sijjnderly^g
Igneous or anatectic material and to
produced by rdatively gentle orogenic defon •Willard's report. The country rocks consist
fgarnetiferous quartz-mica schists, quarliitc,
tion. Granitizing fiuids developed leucog
some of which consolidated in place; some i "ble, phyllite, and amphibolite. The phylcarry metacrysts of staurolite, and the
mobilized and travded along foliation f
and fractures in pardy granitized raeti
ments to form sillsand dikes, A stock of (,
diorite (5 square miles) with sharp cent
steep walls, and a flat domed roof intrudes I
schists.
sociated rocks contain randomly oriented xenoliths of schist and quartzite.
The metasedimentary beds are part of a
homodine on the east limb of an anticlinorium.
EXPLANATION
f
Pinions of Shuswap Coinplcv, British Colun
V
V
V Cwg V
Wiiliomsburq gronodiorile ond
ossocioled pegmotile
According to Cairnes (1940) the area of
Shuswap complex may be more than
Cbt
N
square miles and consists of intensdy nn
4>
Belchertown
tonoltte
V
V
V
v
V
,
Ro'
p
p
V
r
\
r
°
fei
morphoscd Precambrian beds of Belt (?)
about Shuswap Lake, but in other areas
indude Upper Paleozoic and probably Trii
formarions. The metamorphic complex
Phylliles, schists, quorttile,
morble ond omphibolite
tains abundant pegmatites, gneisses
aplitic injection material as an important
stituent, great bodies of granitoid gneiss,
sivc granite with many bodies of pegmatiti ..
Strike and dip ol (oliolion
granite, and a "sill-sediment" complex «
(onqle of dip, verlicol)
crystalline schists and sill-like bodira of gtanil '
gneiss. He believes that the prindpal process -1
have seemed to mvolve a gradual upww ':'Strilte ond dip o( second
seepage of this material (pegmatitic and aplitj
deformation slip cleovoqe
differentiates), infiltration along beddingplanq ^
replacement or partial replacement of inltt '
vening rock matter, and the growth, in sil*, ;
of perhaps.much of the pegmatitic granite. Bi
suggests that, in places, the continued suppi)
Isa-ss
of magmatic material resulted in the coraplet
SCALE IN MILES
conversion of large bodies of the original stnl
into massive granitoid rock, which, under
conditions of transformation, became pai
plastic or molten and, where subjected to
FIGURE 12.—WILLIAMSBORG GRANODIORITE PLUTON OP TRANSI-HONAL MESOZONE-CATAZONE
stresses, behaved much as a normal intniaAppalachian orogen, Massachusetts. Modified after Willard (1956)
rock behaves in its contact relation with
joining rock masses. Cairnes bdieves
ists locally have metacrysts of staurolite The schistosity is approximately paralld to
granitization was effected in connection wil id kyanite, most abundant near the grano- bedding on the limbs of folds but cuts across
the emplacement of the Mesozoic bathdii
rite, Sillimanite and tourmaline are de- the bedding on the crests and in the troughs.
Armstrong and Roots consider the Shuswajipoped near contacts with the intrusive rocks, The axial-plane schistosity is inferred by
complex the equivalent of the Wolverine cwhSie amphibolite consists of hornblende, un- Willard to have been deflected at the north by
plex and date the granitization as pre-PennS}winned calcic plagioclase, with quartz, biotite, the force of the intrusion (Fig. 12). Slip deavage
vanian or pre-Mississippian.
mite, and epidote. The rocks may barely is a planar structure that coincides with the
ive attained the staurolite-kyanite facies at axial planes of small corrugations or micro^e time of magma emplacement. The grano- folds in the schistosity. For the most part the
Williamsburg Granodiorite Pluton, Massachu
orite is in large part a mixed type consisting slip deavage is parallel to the exposed contact
The Williarhsburg granodiorite pluton in I ibiotite-muscovite granodiorite and of pegma- between the granodiorite and the country rock.
Williamsburg quadrangle, Massachusetts,
|e, granitic, aplitic, and granodioritic dikes This suggests that the schistosity planes nearest
scribed by Willard (1956), appear^ to be^fti |0d sills of many sizes. Some of it might be the intrusive moved up rdative to those farther
example of emplacement under conditioi "ed an injection gneiss. The granodiorite is away, Willard believes that,.in large part, the
transitional between those of the mesoa ^Irnded by granite and pegmatite dikes and intrusive forced its way along earlier foliation
jridj^atazone. The following abstract is
us. At many places the granodiorite and as- planes, bending them apart, causing the de-
and producing local shear couples-that resulted
in the slip deavage-that surrounds and dips
awayi from it. The schistosity planes hearest
the intrusive moved up relative to those farther
away. A northwest-trending slip deavage was
produced by a; la.ter deformation. The preseiit
writer would also emphasize the discordant
relationships betw'een the- borders ot the intrusiveand the country rock, as portrayed both
in plan and by the section £is drawo by WQIard,
that relate this pluton to the mesozone,
{and Nonewaug Granile Lens of
Mesozone), Comtectictd
j
',
A b d t of rocks in Connecticut, region^f
metamorphosed in^ the epidote amphibolite ot.
stau rol i te- ky a ni te fades,, co n ta i ns pl u totf
whose characteristics are those of the mesozone.There arc -also bodies of gneiss* formed bj,
migmatization and granitization that, seeffl J |
best dassified in the transitional mesozone- f;
catazorie.
The Paleozoic Nonewaug granite lens in tliH
belt has been described by Gates,,(1954). Thtlj'
Lithmiia Gneiss .(and Stone Mountain Granite, pluton is 9 miles long and 3 miles wide. The]
of Mesozone), Georgia
long axis is about N.60°E, and is across
foliation of the schists whose regional trend]
The Lithonia gneiss and Stone Mountain is north. The schists adjacent to the lens 0|
granite in' Georgia afford another example of a, the north and west borders have in general e
gndss with characteristics of the catazone in- foliation paralld to the border of the granitt
ferred to be associated in tiriie and space with as a result ot crowding aside al the time,(|
a, pluton apparently emplaced in the mesozone. magma' intrusion. On the south border
The- Rb/Sr age of the granite averages 278 foliation of the'schists is normal to the contacH
tri.y. and biotite ^from the Lithonia gneiss The southern part of the granite lens, hdweyet/j
gives 297 m.y., (Pinson ei oi,,. 1957, p. 1781). is a complex mixture predominandy of granit^l
The Stone Mountain pluton 'has been de- pegmatite, and granitic gneisses with subordij
scribed by Herrmann (1954) from whose, work nate fddspathized schist and sdiist. The lolH
the following summary is taken. The country ation is variable, as in a crumpled zone. The'
rock is regionally metamorphosed and consists granitic gneisses are granitized schist, Tbt-|
of schists of the staurolite-kyanite or epidote, bulk of the granite mass has a layered structure
amphibolite subfacies. The muscovite granite dipping 3S°-^8()° SE. and is inferred to be 4.
.pliiton in part cuts discordantly across the magmatic origin. The granite has crosscuttingi
structure of the country rock and in part apophyses and also occurs as dikes in the schists.'
crowds the country rock, to one side. The flow Pegmatite veins, are present in the sdiistt;
structure of the,granite is in part conformable The ribrmal schists are mica quartzites and
to discordant contacts with the intruded gneiss.. quartz-mica schists with biotite and muscovitej
Pegmatite dikes:are locally abundant in the and accessory garnet, staurolite, and kyanite.)
schist on the nbrtfi side of the intrusive, and The characteristics of the pluton seerii appn^
aplite dikes on the south side. .
priateto emplacement in the mesozone.
An independent extensive belt of thfe schist
Stewart (1935) has described from a zone;
was injected and replaced by syntectonic,' southeast ot the.Nonewaug pluton an extensivl
magmatic, potassium-rich solutions' which belt of pprphyritic granitic.gneiss formed in,
modified it to a gneiss (Lithonia gneiss) of
schists ot similar age and grade ot metamorgranitic composition. Pegrnatite dikes in the phism by magmatic injection arid by penne|
Lithonia gneiss are small and irregular; com- ation and replacement by fluids whose souroij
monly discordant but locally partially con- was in a subjacent magma. Agar (1934, p:
cordant aplite forms thin veins, The_ relatiqn- 363-369) has also emphasLzed the extensii^^
ships of the rocks are shown in- Figure 13, The occurrence of mixed gneiss resulting from irt-^
migrnatirizing and granitizing fluids are thought vision of these schists by granite and pegmi'
by Herrmann to be co-ordinate with the magma tite. These gneisses may be the roof portioa'
that formed the Stone Mountain granite. The, of mesozonal batholiths, or they could bdoiig|
rocks surrounding the Lithonia gneiss are to the upper part of the catazone.
metamorphosed to the sillimanite-almandine
amphibolite subfades. I t is thus a problepi to
, the present writer as -to whether the Lithonia Precambrian PhacoUtlis of Hanson Lake. A r i ^
Saskatchewan
gneiss is the roof portion of a mesozonal pluton
or represents an earlier emplacement in the
It appears possible that phacolithic eraplac^
catazone.
ment, although chara.cteristic of the catazoi^
1 • I
U
.A'
M;
1 i]
u
may also occur in tJie transitional mesozonecatazone. Byers (1957) has described several
syntectonic phacoliths of granodiorite or
quartz diorite emplaced in antidinal structures
of biotite gneiss, amphibolite, and migmatitic
gneiss of the Hanson Lake area, Saskatchewan.
The country rocks are described by him as
regionally metamorphosed in the amphibolite
facies or the gamet-staurolite zone or staurolitekyanite subfacies; locally the sillihianitealmandite fades is attained. The antidinal
structures have steeply dipping axial planes
and may be asymmetrical or isodinal.
Syntectonic Piiukneyville Balholith, Alabama
The PmckneyvUle quartz diorite batholith,
Alabama, has been described by Gault (1945)
as a syntectonic batholithic intrusion. I t is
more than 40 miles long, 8-12 miles wide, and
is emplaced in phyllites, schists, quartzites,
and amphibolites that have attained only an
intermediate metamorphic grade.
COMPLEX HISTORY OF GREAT BATHOLITHS,
LARGELY OF MESOZONE
Introduction
Great batholiths such as those of the Coast
Range of Alaska and British Columbia, the
Sierra Nevada of California, Southern California, and Idaho have had a most complex
history. Individual units have been emplaced,
usually in a systematic sequence from more
mafic to more alkali-siliceous, to make up
composite stocks or small composite batholiths.
Such composite plutons have in turn been
emplaced as a contemporaneous or successive
series within a limited period of time to yield
a multiple aggregate that forms part or the
bulk of the batholith. Such series may in turn
be repeated in periods of time separated by
substantial intervals.
The ages of the members of the Sierra Nevada
batholith (largdy mesozone) have been determined by the Larsen method (Faul, 1954,
p. 265) to range in large part between 90 and
111 m.y. and by the potassium-argon method
on biotite to be between 82.4 and 95,3 m.y.
in general.
• The ages of several major members of the
Sierra Nevada batholith in the Yosemite
National Park area have been determined
(Evemden, Curtis, and Lipson, 1957) by the
potassium-argon method. The ages for the
youngest major member is 82,4 and the oldest
713
zuvmruE,.5raT5Wff^J^!raTrBA¥lH6LiTHS, LARGELY OF MESOZONE
95,3 miUion years, a range of about 13
years, and they believe the range is con 1 coarse grain persists to the sharp contacts ciated with Laramide structures and are bept for a narrow chilled edge, in "places less lieved to be product of "Laramide orogeny of
to a few per cent at most. The average intei
1 inch. The description suggests to the late Cretaceous time". He describes a "marginal
of time between successive intrusions is (
ent
writer emplacement in the epizone, facies", a gneissic quartz diorite along the
mated as 2 million years, and each is info
I this is in agreement with his own observa- western side with scattered roof masses in
to be almost completdy crystalline at
more central areas. The gneissic structure he
i of this rock in the Hyder district.
time of the succeeding intrusion. The aull
takes to indicate emplacement during orogeny.
[fer refers certain dome-shaped bodies of
propose
goclase granodiorite and hornblende grano- An inner facies is largely quartz monzonite
"that room for the batholith was made sIowljTi
ite to a Jurassic age. The characteristics without gneissic structure emplaced after oroin small increments by vertical uplift of the ovi •' consistent with emplacement in the meso- genic forces had ceased and formed under rather
ing sedimentary rocks which were stripped by(
sion as rapidly as they rose. Probably some ol ( ne. He describes as still older a thick sheet deep-seated conditions as was the quartz
earliest granitic intrusions were at the surface.! granodiorite which is gneissic throughout diorite. The bulk of the batholith is believed
the time the last intrusion squeezed into place",
possibly of early Jurassic or Triassic age. to be of these Sierra Nevadan rocks. The present
[jnally
there is an older hornblende grano- writer suggests the possibility that the quartz
The writer would qualify this by suggesi
diorite of the western part of the batholith
-itc
for
which he suggests a Triassic age.
that,this mechanism was only one of.sevi
[The probable emplacement of part of the may have been emplaced in the catazone and
factors in emplacement.
the quartz monzonite in the mesozone.
The ages of several outlying batlioliths wil artz diorite of the southwest border of the
Anderson notes that a younger group of
stholith
in
the
catazone
has
been
previously
the sedimentary rocks have been deteri
rocks, induding diorite (of gabbrodiorite type),
iferred
to.
by Curtis, Evernden, and Lipson (1958)Jj
granodiorite, and quartz monzonite were inrange between 133 and 143 million years, [Mathews (1958, p. 172-177) has described
truded later and resemble the rocks of the
It
of
the
southern
end
of
the
Coast
Range
intrusives of the two different age groups
Boulder batholith and its satellites of Late
itholith
that
comprises
both
plutons
of
believed by the authors to correlate with i
sic or Early (Jretaceous age and two Cretaceous age. The diorite has chilled contacts
separate major orogenic periods—one of
ntons
of post-Late Cretaceous age. The and hypabyssal characteristics. The granoJurassic and the other of early Late Cretai
itter are homophanous. Only one of the diorite and quartz monzonite have features he
age.
infers to be indicative of fairly rapid cooling
The Coast Range and Idaho batholiths i unger batholiths shows a faint flow structure,
and intrusion into the cold older batholithic
that near the borders only.
the complex of plutons of the northeasi
rocks fairly dose to the surface.
I^There are also small epizonal plutons of
section of the Appalachian orogen all
Larsen and Schmidt (1958) state that some
quantitative volume in the plutonic
mesozonal plutons as the dominant elemi
coarse rauscovite-bearing quartz monzonite
Implex
of
the
Coast
Range.
One,
described
but al.so many plutons emplaced in the epi
'Gault (1945), has developed contemporane- and some very fine-grained granite of the Idaho
as youngei- members.
explosion brecdas. A stock of miarolitic batholith have small miarolitic cavities. They
The ages of a granodiorite and a diorite
anite porphyry is intrusive into Tertiary also contrast the batholith of Southern Calithe Coast Range batholith' of southeasj
|yolitic volcanic rocks of similar composition fornia in which the largest unit is about 200 •
Alaska have been determined (Matzko, Jf*
IZarembo Island (Buddington, 1929, p. 275). square miles with the Idaho batholith in which
and Waring, 1958, p. 538) to be 93 and
several units are more than 2000 square miles
m.y. respectively. They note (p. 537)
each. Their statements for the Idaho batholith,
Idaho
Balholith
Silver, Stehli, and Allen have determined
however, are based on reconnaissance only,
mean age of 103 ± 6 m.y. for four early
jThe complex history of the Idaho batholith and detailed work may reveal greater comCretaceous plutonic rocks from Baja
been described by A. L. Anderson (1952). plexity. They interpreted a subordinate porfomia. The Baja California, Sierra Nevid
phyroblastic granite facies as the product of
states that the batholith is composed of
and Coast Range intrusives would thus
Crete masses of granitic rock, some of which granitization of schist. Ages determined by the
in part to be of similar age. The Coast
ic to place under deep-seated conditions, Larsen method on most of the rocks average
intrusives, however, are called Late Jui
liers at much shallower depths. The deeply 108 m,y., but one pluton gave 57 m.y.
to Early Cretaceous in this report.
lied emplacements indude two closdy reted, but separately formed masses; the earlier Complex of Plutons in_ Appalachian Orogen.
Coasl Range Batholith
Mved while deformative stresses associated
Nortlieasl Sectioti
The Coast Range intrusives in norl Sth a major orogeny were still quite intense,
other evolved during the later less intense
A varied scries of plutons occur in Paleozoic
British Columbia are stated by Kerr (IM
p. 305) to comprise nine (more or less) distn Jges. Anderson infers that these masses prob- metasedimentary and metavol(a,nic rocks in
kly had their roots in the same source, but a wide b d t of the Appalachian orogen that
intrusive phases which range in age from
Triassic to late Early Cretaceous. Ken-.S It the granitic bodies introduced under extends north from Long Island Sound and
llower conditions came from a younger prob- northeast through Newfoundland. The plutons
scribes the youngest member, which cuts T'
Py unrelated source. The oldest rocks of the range in age from late Ordovician (?) or Taconic
Cretaceous rocks, as a quartz monzonite
Jtholith were emplaced at the dose of Sierra through Middle to Late Devonian or Acadian
in mafic minerals, homogeneous, and mia
with discordant relations to the country
radan orogeny hence near the end of Jurassic to post-Pennsylvanian,
Plutons nf Tirr^r..-^ o„„ /--l—..^ -"-^
le. The younger rocks appear to be asso-
Signs "^^^^.^ician (7) ^^^e- ^^ ^ known. Tbey
\masses, no
j«.oi«ction
^ t o b c f^- ^yearly
- ; ; e r" l i j^p\ex ' as
„ , 1 » S l u r t h e r s t « f ^ , ^ 3 V - ^^" '
rbe - - ^ J f n t u d ^ i a r e i n t e n e d v n ^ y ^ ^ J ^
the
cata=f"^ f^.Spetature as hvg^^^,^>,,s*l
thecata=f'\^f^,Spetatureashvg^^^,^>,,s*l
tohavehad
t«^P ^, ^^g^^n^
, , ^ n ^ nie
M
to have had aa temv
mew^^ ^^^^^.|
';tedhythe8r^<^^„imurnO^^^^^
^^
batholith. S^^'?
29 m.y. ^^>^°Lts (Willard. T^'^^ -™1 t^i'^iii be at least a
p. i28) ° ^ i pwton. Wassa^^-^^g^^necticut
country . " , amount ^i^ "^^ion and ^
t)otnes
Vc
-—^""^
1956), ^"f^Jx vilve a ^or^P^'Jl which sug(Stewatt, f 2lationships sonj o^ ^^^ ,otne
• •gestemp)ace^«^^^
^'^'''"^ t S ^ ^ i" *^,^ve
' ^ e^^'^„„e.catazone.
e n tentatively .
V m f ^°%ansiUonal tne oz^"^, ^he New
grouped as "^
^^^ states »
^^ectomc
^ • ^ ^ n K ' r v i . o 5 pluto^ f^, - V i e d m.
and that th^ ° ^-^es.
u-thoViths occur
giganiticsAWiW
and bam
^^^^
® Vany ^ n t i e n g t h oi the same
.
throughout *j;^tate13evoman^^^)
3^,.
w^ge ir» as? ^ ' ° ^ , W e s ""'^ „re miaroVvtic
pSnsvWan^- J ; S J s t . ^-^JJ^^y^wioundVeucogramte^'^ ^^-.t, p o ^ ^ T n western t^ewi^°"^ ''"i^ewtoundland.W^'.^^S. reports vn-
,-
Augen
and gran
common.
part ot the B
^^^^
717
tions around the mass in a zone half a mile to
a mile wide contain migmatite. The migmatite
is interpreted as formed predominantly by
fordble granitic injection with some accompanying metasomatism. There is a local development of granite augen gneiss emplaced
partly by dilation and partly by replacement.
The Clinton dome is similar to the BranfordStony Brook dome.
in the sedimentary indusions in the interiot
dip outward from the central axial region and
form a well-defined xenolith dome. The growth
of the dome is bdieved by Runner to have
been from the center outward by marginal
intrusion on the border of a laccolithlike struc.ture. As the structure increased in size, marginal
dips steepened.
^
The formation of the Harney Peak dome
I G N E O U S DOITES OF SOUTHERN EHODESU:
was preceded in the area by overthrust faulting
The Precambrian domes of Southern Rhodesia and recumbent folding. Space for the granite
have been described by Macgregor (1951). He according to Runner was made by domal uplift,
• quotes (p. xxxix) with approval the following lateral spread, and replacement. He suggests
statement of Maufe,
that the domes of the southern Black Hills
'Tt is a general rule throughout the Territory probably coalesce bdow the schistose sedithat the strike of the schists and their foliation is mentary cover into a major Precambrian
larallel to the edge of the batholiths and to the batholith. The foliation, he infers, has been
banding of the gneissic granite. Secondly, the produced by flow in the liquid state, replac
batholiths,.being roughly oval bodies, have curving
margins, there being no general direction of strike ment of bedding, multiple intrusion, and shear-^
throughout the country independent of granite ing of solid granite.- Many indusions were iso-j
bathoUths, Thirdly, the schists almost always dip lated by coalescence of paralld sills and byj
away from the margins of the batholiths, thus intersecting dikes and sills and were never en-i
appearing to be synclmal areas."
gulfed in liquid magma. The age of some granite]
•'
l'
'
^
'
.
pegmatites in the Black Hills has been de-|
; Macgregor suggests that the large ovoidal termined to be about 1600 m.y.
batholiths probably originated as homogeneous
Tectonic domes and folds of plastic crystaUiM\
magmas which ultimately consolidated as flowage,—Quirke and Lacey (1941) have con-:
granite gneiss.
eluded that many complex batholithiclike
Interlayered xenolithic domes.—The term domes with invasive relationships shown by
"stromatolith" was proposed by Foye (1916, their diverse facies,may arise from "mutual
;. p. 791) for "a rock-mass consisting of many plastic invasion of the rock layers by solid
' alternating layers of igneous and sedimentary flow" under conditions of deep-zone deformarocks in sill relationship". The types to which
tion, but this interpretation has not received
it was applied were granite plutons of the much application.
Haliburton-Bancroft area, Ontario (Fig. 14).
NORTHWEST
ADIRONDACK
AREA:
Several|
HALIBDKTON-BANCROPT
AREA,
ONTARIO:
bodies of orthogneiss (Fig. 15) with a com-]
These plutons have a minimum of 20 per cent position ranging from syenite to granite have
of layers of gray gneiss and amphibolite. I t was been described from the northwest Adirondacks
-' inferred that the granite magma was intruded by Buddington (1948, p. 24-30). The rock of
concordantly along foliation planes of the all these bodies has a granoblastic texture and
country rock with a doming produced near the evidences of complete recrystallization undei
I center of the intrusion with outward qua- conditions of high-grade metamorphism. Thej
quaversal dips. Osborne (1936, p. 426-427) are inferred to have structures formed b)
believes that only the border zones of the plastic doming and antidinal deformatiot
batholith described by-Foye contain so many
(isodinal folding at extreme) of original sheetj
indusions.
like or gently phacolithiclike differentiated lay?
BMCK HIILS DOME, SOUTH DAKOTA: T h e folers of igneous rock. There is no evidence ofl
' lowing description of the Black Hills Preany granitization or migmatization in coni
cambrian granite domes is summarized from
nection with the remobilization and develop^
1 a report by Runner (1943). The granites of ment of these domes and antidines as in the!
the Harney Peak area are a composite of many case df the reactivated domes described byj
sills, tongues, dikes, and irregular masses of Eskola, although pressure of rising magma be
various compositions and ages. Within the neath the anticlines and domes may have beeil
•• aria are many xenoliths of sedimentary rocks a factor. The domes are hot rheomorphic inj
/ which in the central part are composed of
the sense that their reactivation has resulted
metalimestone and amphibolite. The bedding intrusive relationships to country rock.
—^r>i-orn>n,anfl-)-.he.aiial-nlanes.of. the isodinal folds
Tectonic domes of remobilization with inlro^
ittction of /«IWJ.—Eskola (1949) set forth a
concept of the development of domes in. a
second period of orogeny which has received
wide acceptance. The hypothesis envisages
a plutonic mass of an eariy orogeny later eroded
and mantled with sediments. During a later
Orogenic cyde fluids or new granitic magma was
injected into the older pluton at the same time
that it was deformed into gneiss with accompanying migmatization and granitization or
palingenesis. The old pluton was thus mobilized
||anew, and associated younger intrusive magma
may display an intrusive rdation to the mantle
rocks.
Eskola (1949, p. 470) suggests that the domes
in Maryland described by Broedel (1937) are
of Such an origin. Precambrian granite gneiss
.was reactivated in Taconic (?) time by intru.sion of granite and granitization. He aJso sugjl-gests that these mantled domes occur in orogenic zones and have apparently been formed
under the influence of horizontal thrust movements, altliough the doming itsdf is interred
to be due to vertical movements of granitic
masses, most if not all of which were caused
by swelling during granitization and soaking
with granitic magma.
In a later paper Eskola (19S2, p. 126) emphasizes that in some domes the element of later
granitizarion is absent or only indpient.
Further discussions of the problems involved
in such domes may be found in the papers by
Kranck (1954) and by Balk (1946).
Phacolitkt
Introduction.—^The term phacolith was introduced by Harker (1909, p. 77-78) for concordant intrusive bodies introduced concurrently with folding. He states that the situation,
habit, magnitude, and form of the phacolith
are all determined by the circumstances ot the
folding itsdf and that the ideal type of phacolith is subject to many modifications, in accordance with the varying mechanical conditions
of intrusion. Harker also suggests that origindly concordant relations may be obscured,
, owing to the igneous rocks becoming involved
|in later folding. The original phacolith described by Harker is a dolerite intrusion in a
relatively gentle antidine. Most intrusions to
[Which the term has been applied since, however, are syntectonic granitic types in highly
deformed rocks and may themselves have been
subjected to strong post-consolidation deformation. The phacoliths arc characteristically much
thickened on the anridinal plunging noses or
in the plunging ends of synclines. They commonly range in size between a mile and ascore
of miles in length and may be up to several
thousand feet" in thickness.
Phacolithic intrusions emplaced in the catazone are common throughout the world and
have been especially described from the Precambrian shield areas. Excellent descriptions
of granite phacoliths in Africa have been
published by Gevers and Frommurze (1929)
and by Poldervaart and Backstrom (1949).
Several North American examples, all of Precambrian age, are reviewed here to illustrate
this mechanism of emplacement.
Phacolillis of Grenville subprovince, Canadian
shield.—Phacoliths are abundant in the highgrade metamorphic Precambrian rocks of the
Grenville subprovince of the Canadian shield
where they have been referred to by Wilson
(1925, p. 397). Osborne (1936, p. 426), and
Hewitt (1953, p. 92-93), and have been described throughcmt tlie Adirondack outlier
by Buddington (1929b; 1948; 1956, p, 115-117),
Reed (1934); Cannon (1937), and Dietrich
(1954). Some of the Adirondack phacoliths
occur in marble, and all have a homogeneous
and narrow range of composition (Buddington,
1957, p. 295), These rdationships along with
others make it highly improbable that they
were emplaced by replacement but rather as
magma. Neariy ail those in the marble, 15 in
all, have come into antidines, most of them
into antidines parallel to the major trends, but
some into antidines or syndines that are crossfolds. Extensive phacoliths. of . replacement
origin, however, in many places accompany
those of magmatic intrusion.
Phacolilhs of Ihe New York-New Jersey highlands.—Phacoliths are also abundant in the
highlands belt of Precambrian metamorphic
rocks in New York and New Jersey. A syndinal
phacolith has been described by Lowe (1950).
The granite occurs as a syndinal sheet with a
greatly thickened trough and one well-developed limb. Lowe infers that absence of
secondary foliation and lack of tectonic fabric
patterns in the granite indicates post-tectonic
emplacement. He proposes the concept of "exchange of space" between the magma rising
and the country rocks.subsiding into the emptying magmatic chamber to account for the lack
of evidence indicating lifring of the overlying
rocks by forcible injection of the granite. The
present writer has studied similar graniric
plutons some miles to the southwest, and for
these there is adequate deformation and recrystallizarion in much of the rock to justify
i^'
II
r-^^*"
EXPLANATION
V
V
V
Grontle,granite 7<eis$ ond
ossocioled pegmolile
Hybrid gronile gneiss,
migmolile and assodoted
gronile pegmoliie
tSPOCf,
<S'00'
Diorite, gabbro, homWendite,
pyrcxenite, onorltiosile;
melogabbro, omphiboSle
Strike ond dip of foliolion
/
Strike of foliotlon
Boundary lines of lithologic
units
v\
Fault ar lineomenl
Ordovician
beds
41'30'
TB'SO'
FIGURE 14. GEOLOGY OF PART OF
-»»-.
'imontarv.and.metayolcanic rocks of Hastings Basin southeast of line of crosses are
'''•''f-facies._Meiasedirnentary and melavoli
AREA, CANADIAN SHIELD
le-grade metamoqjhism and include conglomerate, argillite, and pelitic schists, blue-limestone
of line of crosses are in high-grade metamorphic facies and include migmatites, paragneisses in
f\t' T4qc(i•
schist f r n m Knctr 1 i-l r a n i-r r r v l -r c T \ \ t . frrani^«>c
-
— .
75*15'
44MS'
74-30
144»45
T4"45'
75'0<>
-r
EXPLANATION
I ,r I 1 » tl
Phacoliths o( igneous oloskite, predominonlly
in morble
8V •+ + + + + + + + tf*f'=rvt-4-'lf^>'~ iri
#•//•• •^-f V T " '
5f ^* ^* fel-h:^;t45 -X-r-^^±:^
"cJ -rH4<1'30
[*.-.V'-.i
'--«'-«- 'I
I l"^'"^XI XL«A-
Phocolilhs ond sheels, predominonlly ol pseudoigneous porphyroblostic gronilic ougen gneiss
(metosomotized biolile-quorlz -plogioclose
gneiss)-, some igneous gronile.
. + + + + •••'
,^X+
ji-.;.^f*;.;.;y-.;'«
+ ^ + - f + .-f + + -
;.l'5i;.--*>.-^'V/v
<?:.'^-.-\>«r?.vJi
Phocolilhs, syndinol, predominonlly ol quortzmicrocline gronile gneiss. (metosomolized biotite
quorlz-ptogioclose gneiss); some igneous
micfocline-rich gronite.
te t V +1
W>U-:'-5t? + + * + + + + + f ' I T V ;
^-SSs+y-.--':-.*!^-*^ •^-^-•--'--•••'--•^-'-l^l
!''.::-T7'-f--"tA-^ * * + * * * * i S r ' "
. +++H
Elongole domes, phocolilhs ond sheet ol igneous
hornblende gronile ond subordinole oloskite.
pc-«:-,:«-.-:V>-.'.VJv-.i5iJ>;rf. + + + + + + + ^
•
•.«.'.- •*^.>;»;:.-(:ji;J.--:;.i(.
^
* * * • ¥ * * *
+
* * * *
|W + + + + + + + + -f+ + -t-^-~>+ + + + + ± j t _ ± . i t • -t
Marble, migmolile, porogneisses, quartzite,
ond skorn ot Grenville series; dioritic gneiss,
omphibolite.
+ "^^ J . * " * * + + + + + - +
44-00'
44'00
75*45
^
Aniiclinol cores and domes ol gronoWoslic
syenite-quartz syenite-older gronile orthogneiss;
in port complexly overturned isoclinal lotds.
Strike ond dip o l loliotion
Verlicol loliotion
75"J0-
75'00'
FIGURE 15.—PRECAMBRIAN PLU-TONS OF CATAZONE, Nflj
Phacoliths of igneous origin, pseudo-phacoliths of metasomatic origin, ca
considering them as late tectonic emplacements
and as phacoliths.
A phacolith of pyroxene and hornblende
syenite gneiss has been described from the New
Jersey highlands by Buddington (1956, Fig.
6). I t occurs on a steep antidinal fold, is more
than 12 miles long on one limb with a thickness
amount on the plunging nose' of the antidii
Younger granite also occurs as a younger phacw
lith flanking the syenite gneiss (Buddingtod
1956, Fig. 6) on the same antidine. In the aren
to the northwest of this composite phacolit^
Hague el al. (1956, p. 459) describe phacolW
Bvram orram-to o-—.;— f i — .
-
! < , . 74*45'
74* 30'
loACK AREA, N . Y., OUTLIER OF CANADIAN SniEip
ligpeous domes, and tectonoplastic domes and antidinal cores of orthogneiss
II
lithe Byram gneiss and other rocks indicates
||that the Byram was formed either as a phaco•ilithic intrusion or by replacement of a large
fmetasedimentary sequence and that most of
[the fidd and microscopic evidence points to an
[igneous origin. They condude that the Byram
igneous intrusion coupled with partial replacement.
Phacolithic emplacement of plutons in the
New Jersey highlands has also been described
by Hotz (1953, p. 185-192) and by Sims (1953,
p. 265-268).
TV/l/./ M r m i i t n U r
hhnrr^UlU
T«
described by Stenzel (1936), He suggests that
the granite intruded as a phacolith into the
trough of a syndine that pitches on an average
16° SE. The granite is underlain by gneisses
and overlain chiefly by schists. The intrusion
he. bdieves took place toward the end of the
period of folding of the country rock and was
accompanied by the stress that produced the
folds. Stenzel infers that the feeding channels
of the intrusive body are in a long shear zone,
• which extends along the phacolith and cuts
across the schistosity of the country rock.
Thus the magma, after rising in this moving
shear zone, spread out into the syndine along
the boundary between gneiss and schist.
Harpoliths,—The angle of pitch of the axes
of phacoliths may range from gentle to 90°.
The name "harpolith" was originally introduced by Cloos (1921, p. 44-47, 84-85) for
intrusions of sickle-shaped form emplaced
. contemporaneously with the formation of cross
folds in steeply folded rocks. There are numerous harpoliths in tHe Precambrian of the
. . Adirondack area. The synduial phacolith
, described by Dietrich (1954) could be called
a harpolith.
Replacement pseudo-phacolitlts.—Some phacolithiclike granitic masses are in large part the
- product of granitization and metasomatism,
such as the Hermon pseu'do-phacoiith of the
northwest Adirondack area. New York, and
the sheet of granodioritic gneiss of the Manawan
Lake area, Saskatchewan, described in sections
that follow.
Ambrose and Burns (1956, p. 49-52) have
inferred that the granite sheet conformably
surrounding the Clare River syncline of the
Grenville series in Ontario is of replacement
origin, primarily because of. the general conformity of long thin septae of limestone and
the lack of disturbance which they infer should
accompany magmatic emplacement. The present writer, however, is convinced of the possibility of .essentially conformable syntectonic
emplacement of magma in folded rocks.
Quirke (1929) has described a series of Precambrian intrusives from the French River
area, Ontario, which he calls batholiths. His
description of the structural relationships,
tectonic history, and his interpretation of their
origin, however, permit them to be called replacement phacoliths. The country rocks are
metasedimentary rocks and migmatites. The
plutons consist primarily of granitic and syeniric
- - - ^ k c . J h c m a j o r structures of these areas ac'^—'-''"•!>-iinifvinc
its apex to the north, to which converge anb
iindrical fold resulted from a deformation of
emplacement is considered improbable because
dines, synclines, and fault lines. The batholiti
fiously isodinally folded metamorphic of lack of flow structure or of post-emplacement
conform to the country gneisses of this struc-l
i of the Grenville series that caused rota-' deformation.
ture. The masses of plutonic rock are in generul
small, less than IS miles long and less than 51
EXPLANATION
miles wide. Quirke states that the intrusiv^
lenses are indined to widen along the
Unmapped
region of the great syndinc; indicating thsQ
intrusion and folding were closdy connectcdl
V V \
Gronodiorile
in origin. The granitic rocks appear to him t ^
; V
V
be replacements of sedimentary rocks, and W"
cites as one line of evidence that the pWjji,
L V . V 1 Gronodiorile
/ . V
crysts in some certainly have grown withi3
• 1 gneiss .
1 >l
gneisses which still are easily distinguishaWa
; ~ ~ 1 Homblendic
as sedimentary rocks, and that these gneissew
or biotilic
grade into masses which are so exdusivdy porS
migmolile ond ougen gneiss
phyritic that no trace of other s t r u c t u r e ^
texture remains visible.
Hornblende gneiss
Phacolitliic and pseudo-phacolithic empU
ond gronulile,
ment, Manawan Lake area, Saskalchewaii.-^
omphibolite
Complex phacolithic emplacement appears t y
Biotite and biolilebe well exemplified in the Manawan Lake areas
hornblende meloSaskatchewan. The area has been mapped andl
sedimenlory gneisses
described by Kirkland (1956), and a part d i
the geologic map is,'shown in Figure 16. T M
Melo-arkose
plutons were not designated as phacoliths 1 ^
Kirkland, but the structural data given
Foliation and
consistent with such an interpretation, Tbq
gneissosily
rock mapped as granodiorite gneiss is described!
as a strongly foliated or finely gneissic rocy
'22 Lineotion
composed of quartz and feldspar with Hon
blende the most abundant mafic mineral,
many places minor amounts of nodular meti
arkose, biotite gneiss, cordierite-biotite gnei^
103'00'
and hornblende gneiss also occur. The grano
diorite gneiss occupies the same position on I
Scale in Miles
east side of the Lake Manawan dome C^.M^
fFiGURE 16.—COMPOUND GRANODIORITE PuACOLi-rHS (M.L, AND S.L,) or INTRUSIVE ORicrN AND
as the meta-arkose does on the west side, andj JPSEUDO-PHACOLITH OF GRANoniORmc GNEISS (RECRYSTALLUED AND GRANITIZED META-ARKOSE
the granodiorite gneiss is inferred by Kirkla
IN PLACE), CATAZONE
to be a more highly metamorphosed granitia^
Modified after part of Manawan Lake area, Saskatchewan, by S, J. T. Kirkland (1956)
equivalent of the meta-arkose.
R;
The conformable phacolithidike core ot I
on about a vertical axis expressed by buckling Emplacement in tlie Grenville Subprovince,
Lake Manawan dome consists of leucocrati
Canadian Shield
competent bands along the strike and in
porphyritic to even-grained granodiorite.
iftain places of flowage of incompetent layers
General
slatemeni.—^The
Grenville subplagioda.se exhibits albite and Carisbad-albiu alo "vorrices". The pluton is formed in part
province
of
the
Canadian
shield
indudes a
twins. The rock is generally massive butt
fy gabbro but in large part by monzonite tliat belt more than 250 miles wide and more than
places weakly foliated. The granodioritej
places gabbro, paragneiss, and marble. The 1000 miles long consisting preponderantly of
interpreted by Kirkland as intrusive. *£
iuton is about 15 square miles in area, and the uniformly high-grade metamorphic rocks and
foliation of the country rock is conformable igneous piutons of the catazone. The province
Stdicylifulrical Plutons
•ith the margin of the mass. Numerous relics includes the Precambrian'outlier of the Adiron' country rock occur within the pluton, and
dack area in New York. The rocks of the highWynne-Edwards (19S7) has described
heir foliation conforms to the attitude of the
lands of New Jersey are similar. Many aspects
Westport pluton in Ontario as that of an alma
!ternal mantle. There are several such plutons
of the area are discussed in The Grenville probvertically plunging cylinder emplaced in,!
1 a row close together. The plutons are inlem (Thomson, 1956). Age determinations
vertical cylindrical fold or "vortex" that fon
Ted by Wynne-Edwards to be post-orogenic,
a natural vertical channel for the uprise.'d
(Shillibcr and Gumming, 1956; Eckelmann and
liplaced in a dilatant zone with no indication
~ j / - . „rnniric emanations, T M
fflowstructure. A syntectonic mechanism of Kulp, 1957) lead to the inference that the
I
i i U O Ui. LlIC
auuuieasc respectively and are granobUaCT^Hi.
j
..
^- i^ ..i
general Haliburton-Bancroft area, Ontario,
T n
t I
4. e 4.1 „ k»if IMM.' *"«ern and eastern antidines of orthogneiss
are 800-900 m.y. and 1050 ± 20 m.y. old.
gneisses. In the central part of the belt, not^; ^
t .,
,
•-,. •
,
Plutons in tlie Grenville series of Quebec.—
.,
,
,,.,'^ ..,
• „• J __,^ *W as floors for the phacolithic emplacement
Osborne (1947) has had much experience with ever, there are phacoliths with gneissoid me*, , ,
- , ,
L .L
.L
the geology of the Quebec part of the Grenville
,.
.. "^
.
°
"Ithe younger granite athough the southern
T-u
u J ofcpseudo-Igneous
J •
...porpny*
„«.^t..-»* ^^ " ^, ^ s northwest , limb
The 1largestI. body
,, of the,. northern
.. i belt
..x.
subprovince, and the following statements are
There
are several
syndinal
phacoliths
of
1,
..
•
,.u
o
-11
u„ii
i.
ll*
'
"'"logneiss
was
locally
cut
out
by the
based on some of his conclusions. The type
tz-raicrodine
granitic -gneiss.
These -^repre° .
^
locality for the Grenville series lies within a blastic augen gneiss m the Grenville bdt is IIK
A metasomatized biotite-quartz-plagiodase
dejective zone. Within this zone the intrusives Hermon pseudo-phacolitli (Fig. 15, t A f r i . . . .
(Buddington, 1957) in part and in part
tend to be concordant with the Grenville rocks. 44°25' Long. 75°15' to Lat. 44''08'
75°45')- The rock is predominandy a
Between the dejective zones are broad areas
witli augen of microdine in an even-gn
characterized by schistosity parallel to bedding
gneissic groundmass. The phacolith has n fflb'T . . . . .
, ,
and by gentle dips. In addition to sills in these •
1 .,1. c IC - 1 1
• 1.1 „( i.jr"P'»rtz-microcline igneous rock of magmatic
imuni length of 35 miles and a widtli ol ' ' * l ^ Ti.r i r .i
.
.. • -n..
rr,
-..„
„,
iwl*?'"Much
of
the
metasomatic
rock is silliareas there are batholiths of coarse-grained
miles. The granitic mass is continuous at »»L,,-,, r,,,_ ,., .....
^ i - i
.,
: °
, .,
,
.
,„ „f „ ^i-P^^'t'c, The biotite-quartz-plagiodase gneiss
granite tliat cut across the structure. Osborne southwest
around the plunging nose of a S8»-| ,
r
, ,. ^^
• j .
notes that some measure of syntexis is observa- ordinate antidine and the tfough of a s y n d i a > C ' f " " ' ^ ^ . i''"';
'""^ replaced to
ble, particularly in the dejective zones, and The granite mass transgresses the trend of a W p ""= Porphyroblastic augen gneiss m the
gneiss
fromare)
oOti , • ...
^i. ,.
.. t ..i.
that members of the normal sedimentary series of
the biotite-quartz-plagiodase
gneiss
.,
rto,,marble
, .,at the, , base.
,1 There
„, „„rt j j ' t i tic
e complex and
in the southeastern part
of the
one side ofbetween
tlie stratigraphically
upper
partoi , domes
,r\ - .i antidinal cores
J fof. grano.
may be missing, in which case a variety of gradarions
porphyroblasts
in the
orthogneiss
of an composed
eariy period;
igneous
'
J ft- •
.aa,ilic^p,
J5J
j^j^
of tectonogranitic rock occurs in its place. He suggests tite-quartz-plagiodasc " gneiss,
porphyrobla
les, phacoliths and sheets; and pseudothat magma appears to have been tlic dominant schlieren of the country rock in the gr
icoliths
of metasomatic granite gneiss.
constituent of the syntectic but that at a few mass, and uniform granitic augen gneiss, M\|
Plutons of Haliburton-Bancrofl area, Ontario.
localities the granitic gneisses were formed by matic facies of the biotite-quartz-plagio
granitization of paragneiss. In the Ottawa gneiss are also associated. The granitic gneisi •The study of the Haliburton-Bancroft area
folded b d t Osborne (1936, p, 426) finds that variable in composirion, A syenitic fac'es is 4 Ontario by Adams and Barlow (1910) has
e this a classic area for the portrayal of
most of the intrusives as a whole partake of the veloped locally in mixture with amphit
in aspects of batholithic emplacement. A
nature of phacoliths,
All these phenomena have led to the interpr
ied geological map (Ontario Dept. of
Plutons of northwest Adirondack area, New ' tion that the granitic gneiss is of metasomiti
les. Map 1957b) and a revised interpretation
York.—Several types of emplacement of plutons origin. There is also some even-grained
the geology by Hewitt (1956, p. 22-41) have
in tl-ic catazone are well represented in the associated which is inferred to be of direct
stnUy been published.
Grenville series of the northwest Adirondack matic origin. There are some bodies of ine<j#CL , , . / , . ,
,
.
,.
,
area, New York, and outlier of the Canadian
, "
-,.
-.
- „ -„j„,j~i ki 'lie belt of high-grade metamorphic rocks
irlhwest of the Hastings Basin (Fig. 14)
shield. Representative structural relationships granular granite or granite gneiss intrudca ' ' ^.^
° °
, ,,, J
^,
. ,,
t. -.1 i^«*'i'des marbles and silicatcd m;
are shown in Figure 15.
isolated sheets in marble. These may repres«rf . ,
j -i- ^ j
.i
u •
remobilized orpartlv anatectic material, D«. ,
' - - - d orpartlv anatectic material, b * J^^^ " ' ^ f ^ f ^"f sd.catcd marbles basic
In tlie northwest part of tlie area is a belt ,
... i - l
rri .„i..i;nM '•came rocks largely altered to
about 25 mDcs wide in which members of the we have no critical evidence. The soluli-3^°''"<^ ^°<^s ^^'S^^y ^^^^^^ t° amphibolite
we have no critical evidence. Ihe soluiMi* ,.
. " -'
,
,,
,
Grenville series are predominant. The granitic
elTecting the metasomatic devdopment ol li* ^ f ^""^ ^ " " ' ' ' ' ' " l ^ ^ f f ' ' b r o / n d metaplutons occur as alaskite phacoliths of intrusive
augen gneiss are interred to be rdated to rai^'« gneiss paramph.bolites, and paragneiss
magmatic origin, mostly in marble, and as
m-itir n-.i^<;e<; bdnw
.v|"'*'"'"g sUlimanite and garnet. Hewitt desheets of porphyroblastic augen gneiss formed
matic masses ueiow.
-x'. p^-i ,, , ,, i.., . ,i , • i
j
largely by metasomatism of biotite-quartzTU i
^
c ll
J _• •».! t,., •*• ™^ the batholiths in the high-grade metaplagiodasc gneiss interbedded with marble.
The structure of tlie area dominated by C" ,,^, • ,
. ,
t
•..•
. ••
Most of the phacoliths have moderate plunging ncous rocks, pseudo-igneous rocks, and orlb^ ^ ' c terrane as mixtures o granitic material
axes parallel to the major trend of the forma- gneisses in the •southeastern part (Fig, IS) W ^ " g from granitic gneiss to pegmatite mtitions, but a few are in crests or troughs of cross- been controlled by the antidinal folds a< » % "Uected into and replacing paragneiss
folds plunging neariy at right angles to tlie domes of granoblastic syenite-quarU syen,> J amphibolite. Abundant indusions and
trend of tlie formations. The phacolith at the older granite orthogneiss that have served H 2^^'» ^'^ P/s^^.t. and gradational hybrid
Mtism.
extreme nortliwest is emplaced in a cross-fold rdatively rigid butfresses. The metamorphic J'^
of mixed o„g,n are common. Most of
plunging southeast in beds isodinally over- and deformation of these rodcs along with l i t ^gramuc bodies are concordant, and there
Molithicevidence
Development
of Pseitdo-igneus
turned to the northwest with steep dips. Sev- r,
,,,
t u J
„ i„j •u^ »,«nl./».?''"ich
of granitization
and Granite
metain Catazone
eral small phacoliths along the nortlieastern Grenville series of beds preceded the empiwt-*
^
half of the southeast border of the Grenville b d t ment of the younger granitic plutons. Ttej
are also on cross-fdlds, here plunging northwest. magmas yielding the syenite-quartz syenB*'| [ Introduction.—The occurrence of replaceKnt pseudo-phacoliths and sheets in the cataThe phacoliths along the northwest and south- older granite rocks are inferred to have
east portions of the Grenville b d t arc in zones emplaced as relatively flat-lying sheets *! oe has been discussed. A few examples
gently
ern
limb
transitional
part
of dipping
an
of the
antidine
epizone-mesozone.
western
phacoliths
overturned
belt of
of orthogneiss
the
The
to epizone
the
northi
sovB4J
liths will now be considered. Many have been
described from the Precambrian, especially the
Canadian shidd. Early papers advocating the
emplacement of batholiths by replacement and
recrystallization were those of Quirke (1927)
and Quirke and Collins (1930). Some recent
examples are those of Harrison (1949), Christie
(1953), Robertson (1953), Steven (1957), and
Eckelmann and Poldervaart (1957).
Harrison (1949, p, 34-39) described the rocks
of the File-Tramping Lakes area, Manitoba,
and conduded that granitization has locally
affected all volcanic and sedimentary formations in the area and that it has taken place on
a regional scale and has locally been intensive
enough to produce granite. He infers further,
however, Uiat abundant evidence indicates
that magmatic granite also existed in large
amounts.
Robertson (1953) has described the rocks of
the Batty Lake area, Manitoba, He finds that
gneissic, granitelike bodies occur in the Batty
Lake area as bodies of batliolithic size, as
stocklike and sill-like bodies, and as pegmatite
bodies. Viewed in aerial photographs, the larger
bodies exhibit complex to broadly sweeping
folds resembling those of sedimentary formations, but in the outcrop they are granodiorites,
tonalites, and granites, compositionally, with
well-defined foliation and grading imperceptibly into rocks, apparently of sedimentary
origin. He condudes that "granitization"
commences with the development of albiteoligodase in the sedimentary rocks, producing
rocks mapped as "granitized" gneisses, and
continues with the later formation of microdine to form bodies of granitoid gneiss that
may, in some instances, have become mobile.
Robertson suggests that the cause of regional
metamorphism and "granitization" in this
area is the proximity of magmatic material at
depth.
The development of quartz monzonite gneiss
and extensive granite pegmatite veining by
metasomatism has been described in detail by
Steven (1957) from the Precambrian of the
Nortligate district, Colorado. The country
rock is hornblende gneiss, and remnants are
abundant in the quartz monzonite gneiss.
Metasomatism has been effected by tenuous
silica- and alkali-bearing solutions. The gneiss
is inferred by Steven to have locally become
mobile, moved as a plastic crystalline diapirlike
mass, and developed with its foliation in the
form of a funnel.
fSfniRasicatdiowaii shows very well the kind
of phenomena that have led to tlie inference of
batholithic emplacetiient by metasomatism.
The fpliowing description is based on that ot
Christie (1953), and two selected areas trom
his map arc shown in Figure 17. Mote Uian
50 per cent of the Coldfietds-Martin Lake
map-area is underlain by a complex of "granite,
..granite gneiss, and granitoid gneiss. Christie
concludes that the granites have been emplaced
mainly by a granitization or replacement
process, although various; small bodies such as
the Mackintosh Bay granite may have, been
emplaced as a,molten magma. The. Mack in tosh
Bay stock is shown in tlie lower pact of area.
B" of Figure 17, and Christie des'cribes it as
fjrieissic with the appearanfce pt having thrust
aside tlie eiiclosing .sedimentary, strata during
emplacement. The foliation of the.granite,iiear
the contacts is everywhere parallel to. them.
Witlvin th"c stock the foliation has a rough
elliptical plan, and lineation indicates a plunge
of about 35° SE.
.Christie states'that in general, although the
con tacts ot granitic rocks and ai'n phi boll te are
sharp, the codtaGts, with quartzites'are commonly gradatipnal o-ver tens, hund reds, or even
thousands of feet; Typical coarse-grained pegmatite dikes- or sills are rare except in the
me tase d i me n tary r ocks nor th a nd no r th wcs t
of the M'ackinfbf.h Bay granite stock:
TKc foliation of tlic.granitic.rqcks-ncar contacts with metasedimentary rdics dips gently
or moderately Ijut tends to" be steep or vertica!
.away from them.
The evidence for emplacement of most of tlie
granitic rocks by granitization- is based by
Christie largely on gradational zones with
quartzite, evidence for a conijilcx series, of
replacements indicated by interpretation' of
micrptexture, and tlic Lick of displacement,of
most relict structures. The latter is exelnplified
by the iiidusioriB outlining a skeletal told in
the upper part of area B of Figure.l7,
Qiiad Creek :area, BcatSoolh Mottiiiains, Montat'ia.^A detailed study of the Quad Creek area
ot Precambrian age in the Beartooth Mountains has been published by Epkelinann and,
Poldervaart (1957). Age determinations ot
these rocks byGast and Long (1957) based on
&b-Sr place them, iii general between 2730
and. 2800 m.y. The following description is. a
summary based on the" report of Eckel mahn
and Poldervakrt, The Beartooth Mountains
foriiT an elongate range with longer axis trending northwest and consist of a; core ot granitic
_Rrieiss flanked by migmatites and metasedi-
m'ents. The historical developraeiit is bdi
to be (1) original deposition of an Ardiean
mentary sequence; (2) emplacement of tni
gabbro and ultramafic intrusions^ followed
folding—told axes strike north-northeast;
regional metamorphism and granitizati
resulting" in a.core of granitic gneiss and nu
of migrnalites and metasedinicnts with li
danes'trendiiig northwest. The l.'ist eipri
of grainitization was the production of P'
ti tes, E ckclmann -: a n d Pol d e r vaa r t, be! ie ve
their studies indicate in-place formation
graiiitic gneiss. Fold axes pass continuoi
and without deflection from the ifiant
metasedirnents and migmatites across
boundary zones into the core of,granitic gni
altliough the folds intersect the boundary
at 40° to '50°-, The boundary zone consists^
in ter sec ti ng, to n gu es, raigni ati tes, a tid g rani'
gneiss, and these rocks grade into-each d
along and across 'the strikCi In tlie boundii
zone more-resistant rock types persist at d]
nite horizons, continuous- with skiatiths
similar rocks in granitic gneiss. Throughfolia tion in granitic gneiss-and banding^in
m ati tes parallel bedding in metasediiiieiil
Growth phenomena shown by zircons otdi
eiit rocks they believe also indicate autoch
nous formation ot granitic gneiss at teni
tures probably about .500''-600°C. Eckdm
and Poldervaart conclude that granitization
effected by migrating-alkaline'aqueous
tions during a prolonged Arcliean cyde
thermal activity.. The following., statement
also from their description and from a pei^w|
com liiunica.tion trom Poldervaart. The roctt:
of the core consist mainly of granitic giiei
in part showing banding, with many migtt^j
tite layers and some mctasediniEnts. The
cons are a rounded type with overgrowths
outgrowths. The niore homogeneous granil^
facies, in particular, have some euhedral
cons. The rocks of a boundary of transititWj
zone comprise migmatites and granitic gnds
witli some metasedirnents. The more.neartj;
.homogeneous granitic facies have zircons like,
those of the core, whereas those of the mote
inhomogeneous areas-are similar to those of ths
mantle. The rocks of the mantle are mostly;
roigmatites with associated metasedimcnts QBO
some grani tic gneiss. Rounded zircons, rounded
zircon.s with outgrowths,-aiid rounded zirconl.
with overgrowths, are all present. The first twoare about equal in quantity. There thus a p p ^ ^
to be a gradation in the' transformation OEHTcpns du'ring granitizarion. The core ot ^'?.
Beartooth block consists predominantly'(^
pink leucocratic granitic gneiss, with tonaiitic
gneiss developed toward the migmatitic boundary zgi-ic.
The authors erapliasizc that field rdations
are critical in establishing the metasoitiatic
hypothesis. Insofar as structure alouc is concerned, however, the- following alternative
in tc ipr eta tion might be posed as a question.
Gould the pluton have been emplaced between
synclinal leaves of" country rock as magma
wedges tliat; were relativdy very thick a t the
soiith and thin at the north sp that a marked
constriction ot the magma wedges occurred
albiig the pseudo-discordant boundary of
granitic core, and mixed rocks? ;SupplEmental
granitization would accompany the magma.
Contplcxily of Precambrian Plulonic Ccunplexes:
Gcneroi,-—-The Precarabriaii plutonic com•plexes ot any area of considerable size riormally
comprise a complex ot granitic plutons that
'have been emplaced in different zones at different times, Anderson, Scholz, and Strobell
(1955) have-described a Precambrian complex
^ of the.Bagdad area, Arizona, where the earliest
\ intrusive members-, are epizonal plutoiis: ot
rhyolite and alaskite pprpliyry, followed by
mesozonal plutons (age 1,600 m.y,) in Precambrian sdiists of inter cticdi ate grade of
metamorphism. KalUokoski (1952) has described" similar rdationships from the Weldpn
Bay area, Manitoba, where a Precambrian
epizonal stock ot fine-gfa.ined granodiorite
with a porphyritic quartz latite border fades,
is interspersed with younger Precambrian
batholithic intrusions that, have developed
niigmatites with adjoining schists appropriate
to the mesozone or catazone.
'CrenviUe 6el(..—The writer has estirhatcd
that .over a third of the igneous rocks (indud. ing orthogneisses) ot tlie Adirondack area ot
Grenville rocks belong to the 'syenite-quartz
syenite-granite series such as form the cores ot
tecto no-plastic domes, and antidines (Fig. 15).
These are inferred -to have beeii emplaced
originally in tlie deeper p a r t of'the epizone altliough mudi of the rocJt now belongs to the
granulite inetamorpliic facies. Granite, perhaps 100-200 million years younger, forms
40-50 per cent q£ the igneous rocks and was
emplaced in the catazone.
The Grenville subprovince in the HaliburtonBancroft area (Fig. 14) includes a belt, the
Hastings Basin, about 20 miles wide, within
..-iiirVi i-'hp Tfirks are of 4 low to intermediate
characteristics, ot the mesozone in contrast*
the broad belts on each side ot high-gra^;
metamorphic locks with plutons of thecatazi
The rockSi of the, Hastings Basin consist Bl
part of the Hastings series, which is thoui
by some geologists tp be younger than
Grenville series, but by other geologists to
part of tive Grenville series. Hewitt (1956i p l
30) -writes that
"The Hastings Basin consists of a terrane ot k
to intermediate igratie of meta morphism, iiicluiuii;
schists, argiUltes, -ivell-bedded blue iiniestor"'
cfystaUine limestones, and volcanics, .Sedimenl
and volcanic structures such as crossticdding, pMt
gradation and pillows, arc frequently -B'ell jw^
-served,''
The basic lavas trequeiitly belong to the l o *
grade ddorite facies. Hewitt describes the De?
loro granite stock as consisting ot a fine^-ll
medium-grained granite with sharp conlacttS
and the McArthurs Mills granite stock a s , < ^
sisting ot a massivei coarse-grained granite wita;
irregular shape arid discordant structural i%^
lations to the country rock. The .intruai*
plutons in the Hastings series thus have boii.
concordant and discordant contacts, and manp
have a contact-metamorphic aureole chat^
acteristic ot the mesozone. The present writflj
notes that the Mar in ora metasomatic iron-ortdeposit is a fine-grained magnetite-pyroxene *^^J
epidote tactite of a type normal for the uppe^^ - '
part ot the mesozone and dissimilar to Mchar acter ist i c ro agn e ti te-b ear ihg- sk ar iis -, ia
the Grenville rocks, ot the-catazone.
Coltn'ddo Front Rtinge.—i?ortions ot
Precambrian complexes in the Colorado FroK
Range have been intensivdy studied and afloidan excellent example of their complexity
The oldest country rocks of the area no*,
consist ot high-grade' metamorphic 610111**;
sillimanite sdiists, quartz-bibtite gneiss ani
schist, quartzite, and hornblende gnei^ affll^^
amphibolite. The sill im an tte-bea ring rwiij
have more, aplite, and pegmatite.
Plutons of the catazone are wdl exempUfiw
by the quartz monzonite gneiss (Fig^ IW i
bodies, Lovering and Goddard (1950, pdescribe tliesc rocks as concordant and neany.i
everywhere parallel to- the foliation, with vrm*'
developed gneissic structure, dosely aS50Q"|
a ted lenticular bodies ot pegmatite, and to*]
tense [t£-^ar-Ki injection ot inclusions of schttl
with some assimilation. I t may also be nolw,
that a few miles southeast ot Central City
quartz monzonite,gneiss has typical catazoari,
phacolithic relationship to a complex isodiwl
•- • i ^i-,._.
:tK;.-. linrnhletide gndat;
i
>
A
Phacoliths also occur within the schists of
the Frecland-Laniarline district to the west
described by Harrison and Wells (1956, p. 54)
as mostly bodies of biolitc-muscovitc granite
that are generally concordant, although some
arc sharply discordant. Many of the bodies are
hook-shaped and crescent-shaped in their
surface exposures and are in the axial regions
of folds.
Boos and Boos (1957, p. 2615-2617) state
that the probably related Mt. Morrison quartz
monzonite gneiss is in part saturated with
ill-defined pegmatite; they suggest that it is of
granitization (palingenesis and metasomatism)
origin.
The Boulder Creek granite (Fig. 18) is
described by Lovering and Goddard (1950,
p. 25-26) as a quartz monzonite to sodic
granite slightly younger and less metamorphosed than the quart,z monzonite gneiss
previously discussed. The granite is furtlier
described to have primary gneissic structure,
less wdl developed but still discernible in the
cores of large masses, and locally with abundant
indusions that rarely show much evidence ot
assimilation. Boos and Boos (1957, p. 26162617) state that no other granite of the Front
Range lias produced so many aplite dikes and
sills. They ascribe tlie granite to a combined
magniatic and metasomatic origin. The plutons
ot Boulder Creek granite are largdy comforraable but in part break across tlie foliarion
of the country rocks. Lovering and Goddard
(1950, p. 52) state that tlie foliation and
lineation suggest that tlie individual plutons
are funnd-shaped, enlarge upward, and are
accompanied by lateral thrusting. Lovering and
Tweto (1953, p. 8-10) on the basis of the
orientation of the primary planar foliarion and
linear structure infer that the batliolith was
emplaced by rise of magma through a central
conduit from which it spread upward parallel
to the linear structure that plunges 40°-60''N.
The schist along the west edge of the batholith
dips under the batholith, but at the north the
granite dips under the schist. The foliarion of
the schist is generally conformable with the
contact, and tlie schist is closdy seamed with
pegmaritc. The present writer suggests that the
plutons of this granite may have been cmplaced in the transition mesozone-catazone.
The Silver Plume granite plutons (Fig. 18)
are inferred by Lovering and Goddard (1950,
p. 28) to be younger than the Boulder Creek
— .^Un hnHie.q.._They_ .statc_that these granites
mesozone-catazone. The Proterozoic
to the generally concordant habit of theiM
sions, in part (Geological Survey of
intrusives. They suggest many local centi
a. Maps 1024A and 1024B), show crossintrusion and that in some places the (
; relations to the country rock and may
of granile masses fed from relativdy^
i to the mesozone. In part the Proterozoic
scattered conduits at deptli has resulloU
ftcs (Henderson, 1948, p. 47-48) are
composite batholith. Boos and Boos (f
uibcd as associated with porphyry that
p. 2616-2618) have suggested that the:
!y seems to grade into the granite and to
Plume granite plutons were emplaced bW
nelically related to it but in places is cut
gressive magmatic stoping.
--'Jf
H&e granite wilh sharp contacts. Henderson
The Longs Peak-St. Vrain batholith haS»
that no method has been found to
corrdated by Boos (1934) with the-r
Bguish one granite from the other e-xcept
Plume plutons. The present exposures
critical structural relationships can be
sent the roof porrion of a batholitli, and 1
nincd.
describes it as a "pine-tree" type of >
ment effected by lateral spreading airij
par-lit injecrion of the adjacent and ovt
COMMENTARYbeds with local folding and rilting, altl
the initial conduits were made by stop«S"|
;, General Siruclural Relationships
deep-seated assiinilarion. There is a gn
shown in the walls of the cirques,
isludy of the literature on the plutons of
feet high, from schist and gneiss at t ^ Jj
America leads to the following comthrough almost horizontal layers of
Plutons emplaced in the epizone,
separating thick sheets of granite, lo i
rially tlie "subvolcanic" plutons with
granite with little schist in the lower^
tly associated volcanic rocks, would proband floors of the cirques.
be classed with the atectonic or postThe Silver Plume granite plutons aWW^
nic group, those of the mesozone as
afford an excellent example where ii'S
rtectonic and post- or occasionally latethe upper portion were seen^it might
atic, and the catazonal plutons, prcterpreted as an example of emplacement M
anlly at least, as syntectonic and syntransirional mesozone-catazone, whcrtMJ^
atic. Also the plutons of the epizone
deeper parts ot the pluton have charade^
belong to the "disharmonious" dass as
diagnostic for the normal mesozone.
by "Walton (1955, p. 8-11) in which
A few discordant intrusive stocks of Te
I,is a strong contrast between the energy
age and emplaced in the epizone add
(of the granite and that of the country
complexity of the Colorado Front Rnngt.?
•as evidenced by contact-metamorphic
Mackenzie district, Northwest TerritM
The batholithic complexes of the disU
i exposed plutons of the mesozone occur
Mackenzie, Northwest Territories,
fly in belts of eugeosyndinal rocks although
have been described by Henderson
tare in general post-tectonic. Those of the
as consisring of both Arcliean and Prole
ne, however, occur (I) in the eugeosynintrusions, each on a large scale. Thei
Ibclls; (2) in belts of miogeosyndinal
batholithic portion intrudes a series ofuW
I and structure such as the Sierra Madre
sediments and metavolcanics but is &Kr
ntal of Mexico {cf. Concepcion del Oro,
places overiain unconformably by
• 6); and (3) in the Colorado, New Mexico,
series of Proterozoic formarions with^S
|,Soulhern Arizona Rocky Mountain belts
conglomerates. These beds in turn
^
unding the Colorado plateau where the
truded by granite batholitlis. Both ddaji
Dents are of mainland or intracratonic
younger groups of rocks have membear
ndinal and shelf types and the intrusions
belong to only a low-grade stage of
dc with belts of faulting and uplift
morphism." Henderson has not discuss*
over, Santa Rita, and Organ Mountain
mechanics of emplacement of the ball
Poos, New Mexico).. The epizonal plutons
The writer notes, however, that the
ralso occur in transverse belts such as that
batholithic complexes in part at least ^
Elbe
Boulder-San Juan in Colorado (Fig. 5)
to show (Geological Survey of Canntb^v
rone including and extending northeast
581.^,) domal structure and that roigai
Ihe Boulder balholith in Montana. The
- - « . . A „ l U"11
O l | Hp-vdonedjn association *tA«
oicjrid^Iesozoic sedimentary beds may
locally be so thin that Terriary intrusions in
Precambrian rocks . arc exposed. Tertiary
epizonal plutons of the Oregon Cascade Mountains occur in very gently warped Tertiary
lavas and in the Cascade Mountains ot Washington in lavas and in folded Tertiary sedimentary beds. The quesrion arises as to whether
the epizonal plutons outside the eugeosyndinal
belts would pass downward into those of
mesozonal type. Ewing and Press state (19S7)
tliat the tliickness of the crust in the Canadian
shield and central Interior Plains is 35 km,
whereas it is 40-45 km in the western Great
Plains and Basin and Range province and
50-55 km in tlic Rocky Mountain region.
This permits the possibility that the Tertiary
plutons of the Basin and Range and Rocky
Mountain provinces are connected with deepseated processes. A mesozonal batholith may
also occur in an old orogenic eugeosyndinal
structure but may have beevi emplaced following the development of amiogeosyndine or
other type of structure in the same region.
A general discussion of the hypothesis ot
granite by granitization has been published by
Perrin and Roubault (1949) and by Perrin
(1954).
Dickson (1958, p. 35) has proposed that
magma emplacement may take place by a
process he calls "zone melting". This involves
crystallizarion ot the base of a column ot
magma to yield latent heat that is in part
transferred by rise of fugitive constituents
(mostly H2O) to the top of the column where
melting of the roof is effected. The differential
concentrarion of the fugitive consUtucnts at
the top ot the magma column arises in consequence of the tendency for such materials
to move to zones of lower pressure and lower
temperature. The quantitative role of the
effectiveness of this mechanism of emplacement remains to be determined. There is the
problem of adequate time and appropriate
physical conditions. I t may be a possible
accessory factor under favorable conditions in
acccntuaring differential
incorporation of
rock with low-melting consrituents thereby in
turn increasing the potentiality tor piecemeal
stoping and in increasing the intensity of
conditions at the roof ot mesozonal batholiths.
Reynolds (1958) has summarized in an attractive manner a stimulating hypothesis that
involves a combination of granitization and
diapiric rise in deeper levels with movement
by fluidizarion and magma development in
the upper levels. She writes (p. 382)
I
I
"As a diapir rises, rocks which at a low structural
level arc obvious migmatites become more and more
homogenized by the mechanical kneading caused by
superposed niovemenls (Wegmann), and by chemical interchange (with npjiropriate additions and
subtractions, and recrystallization). Jn this way a
migmatite ri.sing in diapir style becomes gradu.illy
transformed lo nebulite (Scdc'rholm) and eventually
to homogeneous granite. If recrystallization outlasts the movement then, just as in salt-diapirs, all
traces of the movements will be lost,"
and p, 384
"It is, however, only where granile diapirs have
reached the zone of fracture that cDidcnce of melting
and the birth of acid volcanics has so far been
found".
If tlie writer understands this hypothesis
correctly it involves two assumptions for which
we must await adequate support: (1) that there
is time for a substanrial flow of hot matter to
diffuse upward through the diapir, and (2)
that in the upper zone sonietliing is postulated
to happen that affords energy to raise the
temperature of solid material to tlie melting
point and to supply adequate latent heat of
melting to develop magma. The present writer
considers it at least equally reasonable to
postulate that hot matter diffusing upward
from depths would help to liquify graniric
material in the regionally hot catazone before
that in the much cooler upper zones. The
hjTJotliesis of magma from depth to surface
has advantages witli respect to ease of effecring
homogeneity and adaptability to explain the
systemaric composirional variations of the
different units of composite batholiths and
their structural details. Efforts to check on such
hypotlieses as that of Reynolds, however,
would doubtless lead us to new insights.
The epizonal stocks and batholiths have been
emplaced at one extreme by columnar subsidence with a 360-degree ring fracture (Ossipee
pluton. New Hampshire) and at another extreine by piecemeal stoping of angular blocks
(eastern part of the pluton in Northgate district, Colorado), Subsidence ot blocks for most
plutons probably involves both arc and intersecting angular block fracturing in varying
degrees. The alternative development of
columnar subsidence or of piecemeal stoping
is not related to depth. One factor in aggressive
piecemeal stoping as, contrasted with permissive subsidence may be the predominance
of a tendency for the magma to lift the roof
with consecjuent breaking and subsidence.
^wjc-scale granitization has resulted in batho- but may be thought of as arising from a com"ithic masses. One of the difliculties in proving plex phacolithic mechanism of magma emplaceininitizarion is that nearly all criteria are ment into country rock that has complex
Ebject to alternative interpretations. Much of folds, boudinage structure, and formations
6e rode involved is a leucogranite of a com- much thickened and Uiinned by differential
position approaching that of the experimentally plastic flowage. It is expectable that the magma
ietermined ratio for the major minerals con- will be accompanied by some granitization,
rnned at minimum temperatures with HaO partial fluxing of the lowest-melting constitdeep-seated erosion and of bathohthic em-^^solution. A satisfactory hypothesis as to why uents ot die country rock, and hybridization.
placement in the catazone. This, however, is^ fplacement of varied rocks in an open system The shredded ends of some layers may be due
only partly true, for most of the bathdilhs ot: »y alkalic-siliceous solutions should result in to being squeezed or pulled apart during plastic
most orogenic bdts were emplaced in the aicogranite approaching the composition flowage as well as to irregular replacement.
mesozone (induding Uie transition mesozonfr apenmentally determined to be that of tiie I t thus seems highly probable Uiat metasedicatazone).
1 "^'ectic has yet to be offered. Overgrowths and mentary rocks as layers oi" skeletal folds in
There is only one well-authenticated gred wtgrowths on rounded zircons may dcvdop granite or granite gneiss may be either of
belt ot uniformly high-grade metamorphic " contaminated magma as well as during xenolithic origin in magmatic granite or of
skialithic origin in metasomatic granite gneiss.
rocks with associated intrusives in the whol^P'"itization of metasedimcnts in place.
It has been argued that some batholithic
The problein of the proper interpretation ot
Canadian shield. This is the belt ot Grenvilli
emplacement by granitization has been actype rocks that extends for over 1000 miles" lie significance ot long tliin layers ot country companied by inflation with outward deformafrom Labrador^ to Pennsylvania and is mor^ ^}_ occurring^ citiier as linear sialics ^or out
tion of the walls as the result of introduction of
than 250-350 miles wide. This belt in part hajj
new material. Barth (1947, p. 181) infers Uiat
rocks that belong to the granulite facies and.
Uie Birkdand, Norway, balholith wilh conisalsocharacterizedthroughoutby theprcsenct^etalimestonc slabs in the Harney peak formable walls is a "pelroblast" developed by
of great anorthositic plutons. The ages of the' wtholith is interpreted as xenolithic in in- the introduction of new material as a "doud
granitic intrusives insofar as now determined; ^^sive granite by Runner (1943, p, 449-453), of ichor or migrating ions". Oerlcl (1955, p. 45)
range between about 900 and 1100 m.y. At *''"eas a long thin metalimestone layer m describes the Loch Doon slock in ScoUand as
least part of tiie b d t of Precambrian rocks in P*""^ on Uie border of the Clare River syn- having expanded its volume by 34 per cent
Ihe Rocky Mountains such as Uiat in Mon- '''"e 's inferred by Ambrose and Burns (1956) and (p. 81) "Der Pluton ist durch Metamortana, Wyoming, and Colorado may be analo-: ^ necessitate an origin as a relic in granite phose unter Stoffzufuhr aus pneumatolytischengous to the GrenviUe bdt. Granitic rodcs with Pi^'ss of granitization origin. The mctasedi- Losungen und durch metasomatische stoffages of 2700-2800 m.y. and anorthosite bodies ««ntary rocks outiining skdetal folds in the \yanderung entstanden". The Loch Doon
occur in this belt.
-S Goldfield-Martin Lake area are also inferred pluton has discordant contacts for much of its
The badioliUis of such provinces as tht ''yCliristie (1953) to be rdics in a batholiUi of border. To the writer's knowledge the concept
following, however, were predominanUy em- P=^n'te gneiss of granitization origin, aWiough of expansion of Uie walls as a result of granitizaplaced in the mesozone: the Keewatin provinct' "le present writer would note Uiat some phaco- tion has not yet been advocated for any North
with a width ot more than 250 miles and will, '""c magma emplacement, it not indicated, at American pluton. This is perhaps because
rocks intiuded by granite pegmatite with agcji ''^'^ ^°^^ "ot seem predudcd by tiic rdation- hundreds of examples of mineral deposits have
of 2,500 m.y.; Uie Yellowknife bdt, Northwest^'"PS shown, on Uie map (Fig. 17). Folded ' been studied in which there has been introducTerritories, with pegmatites at least 1850 m.y. amphibolite layers and Uiin amphibolite layers tion of new material, but little or no evidence
old; the Colorado Front Range with son« ™ g™iite phacoliUis of the Northwest Adiron- for inflation in consequence of it has been
granite plutons of about 1000 m.y. age; the- '•^'^^s are interpreted by Buddington (1929) reported.
b d t about 200 miles wide across Newfoundland '^ "^"ol'tlis in granite of magmatic origin,
wiUi plutons of Acadian age; and the zone of- ^''"^as skdetal folds ouUined by layers of
Jui-a-Cretaceous batholiths about 350 mite! wmblende gneiss near Northgate, Colorado
Emplacement of Plutons in Epizone
wide in Alaska and British Columbia. The ?«explained by Steven (1957) as rdics residual
and Mesozone
intensilv of regional metamorphism as indi-; '» quartz monzonite of granitization ongm.
Lava flows, acknowledged by all to be of
cated by rodcs farthest from the major in-! "any recent authors emphasize a skialiUiic
magmatic derivation, may be considered an
trusives is prevailingly that of the greenschist *« contrasted wiUi a xcnoliUiic ongm. Ex
observable large (as contrasted wiUi the size
facies with local zones in the staurolite-kyanili: tensive thin layers of country rock do however
of an ion) base of known origin from which to
occur
in
igneous
sills
(Eckel,
cl
al.,
1949,
Pl.
2),
subfacies. The sillimanite fades is generally
extrapolate to a corresponding magmatic
restricted to zones of rock adjacent to the majoi laccdiUis, and stocks (Murthy, 1957, p. 94).
origin for most plutons of the epizone.
The
conditions
of
emplacement
in
the
catazone
plutons or complex of plutons.
The common occurrence of homophanous
are intense and syntectonic, and it seems
probable that conformable emplacement would structure, the common local development of
Criteria for Large-Scole Granilization
be facilitated. Metasedimentary inclusions miarolitic or aphanitic texture, and the inferred
genetic relationship to lavas of similar comSeveral examples have been described in the in the form of relic folds or skeletal folds in
position associated in time and space all in—<-:.<- : t u „ » K=on r»nst.iil.-i.i:GfLthitI|f?'i'te gneiss are not necessarily "skialiths"
Predominance of Mesozonal Balholillis
in Plutonic Complexes
(
I .,
.1
Jicate tliat Uie Tertiary plutons ivere emplaced
as magmas, largdy or wholly fluid. "Fartravelled" xenoliths from depth and absence
of flow structure in tlie enclosing rock ot some
plutons necessitate a fluid riiodo df tralister
from depth. The magma of Tertiary plutons
was, in the initial stages, fluid enough to yield
lava Rawp, At later stages, after rise to higher
cooler levels in the accumulated lava pile,
loss pf volatiles at lower pressures and partial
crystallizatipn would occur, and the magma
would become viscous enough to "set" before
reaching the surface en masse.
Many geologists have etnphasized the
development of a schistosity that is steeply
dipping, often with subvertical lineation, in
both pcriplicral country rock and in border
fades of plutons, such as most of those of the
mesozone'and many of the transitional epizone:meEOZQrie. Because ot Uiis Uiey have inferred
that the invading material had to be a highly
viscous or a diapirlike mass, partly or largely
•crystallized, rising, upward and dragging its
-wdis; This is probably true for much ot the
quartz diorite facies that tonus the outer part
of many plutons.. Such quartz diorite is reasonably interpreted as thc-product.of incorporar
tion of -country .rode by a more specifically
granitic magma and might the re to re be ex^
[iected to be parUy crystalline. A gain j successive central intrusion of magma could produce, inflation, deform a tion; and up\\'ard, drag
of partly to largely consolidated eariier tacies.
In some plutons.of the mesozone, upward movettient in the border zones persisted through the
very last stages pf consolidation and even into
the solid state.
Such evidence lor viscous magnia in the
border zones, however, does not preclude the
possibility that even initial stages of magma
cmplacemerit in the mesozone may locally
have been trcdy fluid, and it,has iip necessary
bearing on Uic later intrusion of the cores.
Even corifbrmable schistose structure in the
contact zpnes of mesozonal plutons need not
always indicate devdop^ment in consequence of
emplacement of viscous magma. Durrell
(1940) made a systematic study of contact'
metamorphism in the southern Sierra Nevada
and emphasizes that, in contact zones with
granite, metasedimentary phyllites and schists,
may merely coarsen in grain but, retain the
original foliated structure, a mimetic inheritance. This means that if the. material ot a
plutpn of the mesozone were a fluid magnia
in the eariy stages we should not necessarily
exDcct a hornfels to beformeii from metasedi-
mentary phyllites, and it formed it might i
appear subsequently by stoping. It may J
be noted that hornfels, as- distinguished ,'
schist, does occur in the waU rock of
mesozonal plutons. In part, however,
hornfels may itsdt be deformed-at later!
of magma emplacement.,
Mu'di of the gneissoid granite does nots
the amount ot crushing and protodastie.!
ture that would be expected it flowage oc
at a late stage of consolidation. Free!;
pended crystals in an early stage of cryt
zatioii may be oriented by flowage, and
orientation may be preserved and inherit^il
subsequent overgrowUi and control ot ayt
1 i za tio n by th e early f ab ric.
It.secms probable that much,.it not mo^y
tiie magma that yielded the roeks olj'
mesozonal plutons was predominantly Uq
at the time of its cmplacemeiit.
i,"
There is good .evidence Uiat lavas^
locally some., hypabyssal plutons crysta^
wiUi some minera,ls characteristic of m
temperatures than those of their pluH
equivalents (TutUe and Keith, 1954-"MO
and Smith, 1956; Buddington et alj IT
p. 519-522). Most of the plutons, ho«
especially the larger ones, will have crysb
in the presence ot at least part of. their vda
will therefore have remained partly fluid,,!
long time down to temperatures lower I
those:dt lavas, and any initial high-temperi'_
minerals will, ha-v'e undergone recrystalliati
at lower temperatures: The plutons-ta>J
epizone, and their interred rdation5hii»|
those pf greater depth, necessitate, Uiatf
fluid magma that formed them could;"
risen from source to surface in a fela;ii
short tiir.e—a, small fraction of Uie ktiglli|
time assigned to a geologic period. Otl^e
the magnia would have frozen eii route.'
A hypothesis is tliat autodithonpiB";!
parautochUionous batholiths are inet _
in origin, wholly or predominantly splidi^
arose in and ascended from zones now i
in the more deeply eroded areas. This ra^l
problem if we also-assume, as, is here dotWil
most of Uie plutons emplaced in the
and in part in the mesozone were pn
nanUy liquid magmatic. The foregoing I
liteses taken togeUier would necessitate that I
plutonic mass becarrie more liquid as ilESS
into cooler levels and.that.it letfa concenlf"
residuum ot resistant .type of rocks in_".
source area^ the catazone. Rise into'
pressure zones, chemical reactions, and i
in volatiles in the- UDoer Dart ot a
The mechanics of emplacement of plutons
nn (Kennedy, 1955) would tend to increase
in
Uie epizone as a consequence of alternating
y, but it remains to be shown that these
- s a r e adequate to meet the requirements. magma rise with accompanying pressure effects
i iievdopment and rise of granitic magma and magma relaxation with accompanying
ioE the roots ot eugeosyndincal materials appropriate structural coUapse of roof and
i presumably leave behind a series ot rocks walls have been discussed by Anderson (1936)
oscd predominanUy. ot garnet amphibo- and by Billings (194S, p, 53-55; 1947, p, 279jnti magnesian pyroxene-calcic plagioclase 288).
In the mesozone, yielding dt the walls by
ulilc but with some other ,reffactory
Jials. This complex would be appropriately plastic flowage may be expected to be greater
btent wiUi the seismic data for rocks above with depth. This, will commonly' result in
discontinuity in the lower, part ot tlie outward-flaring walls, distention ot Uie root,
Lnot now exposed, but there is no satis- and the potentiality for cqtlapse of local porioiy evidence tha.t Uiere is a concentration tions of the roof over the border zones of the
'iffiistates'' in the now^exjjosed portions ot underlying magnia. This may in part explain
ilcatazone. If erosion has only locally exposed the occurrence ot both discprd,ant and cons deeper tliaji about 12 miles in the earth's cordant boundaries so characteristic of plutons
t, as seems probable, then we conclude that pf the mesozone.
I magma,usually came frorii levels deeper
It is recognized that replacement may occur
1 most now at the surface.
locally with sharp and even discordant contacti;.
.M apparent dominance of lineation, insofar An origin by mechanical rather thaii chemical
I'Skwage structures do occur, in plutons ot processes, hovyever, speras- the best interpre': epizone and the dominance of planar tation for most contacts ot plutons, iri the
ation, with or wiUiout lineation, in the epizone, and Uie similarity of character and
ktons, of Uie riiesozone; corrdate with the probable history indicates a similar mechanical
?nces in mechanics ot emplacement and origin for most'sharp discordant contacts ot
rent conditions of consolidation and flow plutotis in the deeper zones.
JiE two zones. Lineatipn alone appears- to'
The writer finds no evidence tor po'stulatbig a
plated to an early fluid :stage, followed by discontinuity betitveen the compositions, texBJinued crystallization in quiet. In the tures, internal structures, or mechanics of
"' aone continued movement during a. em placement of plutons irt the epizone .and
racted intermediate period of crystalliza- those of therii"eso~zone.There are plutons with
1 permits th.e devdopment of planar struc- iritcrriiediate characteristics that suggest a
P,e in some parts ot the pluton.
series of gradational changes from one to the
liliere appears to be good evidence that some other.
lihe plutons ot the mesozone had extensive
The concept ot the developmeiit df riiigrtiaBfa and could -not have been continuous wiUi inagma with sdiliercnlike structure at the
ttons of the epizone unless tlirough relatively source seeins, reasonable, but its rise and em' i connecting diannds. The plutons-ot the placement "as such" docs not fit the hombphaiMne and epizone locally overlap one or nous core of the plutons: ,bf the mesozone and
tot their bordefs as though overriding them, those of the epiz.one: ti in general tiie evidence for an extensive
The Nor Ui American literature'of. the past 25
J.J is lacking,
years appears to be based on the assumption
Whe.present.data do not preclude the possi- that the best theory, as of the present, for
»tj', however, that the,plutons of the epizone, emplacement of plutons in the* epizone is' one
IScast in part, enlarge downward arid are of block foundering in; or some kind pf stoping
iatinudus with plutons ot the mesozone. If by, niagm> as a major factor. After half a
J.emplacement of. the latter were in sub- century, however, the stoping hypothesis
pntial part effected by crowding aside ot tlie still lacks verification in the sense that we do
'"i then the possibility would exist for em- not, have desirable, supporting evidence of
smcnt of magma in Uie epizone through sunken blocks in the pluiions of deeper levels;
Jdering of crustal blocks into magma bdow; Unless such: blocks have been indistinguishably
ijdomical-pianar or arch-linear structure such incorporated in magma, or rcwdrkcd and
i occurs in some plutoiis ot the niesozoiie metasomatized into new granites at depth, or
"BM form at a late stage in consolidation and have suiik to very great depths, we might
old not nccessarOy indicate a root of original expect to find more evidence of floored plutons
ntrv rock at time of consolidation.
than has been reported.
I, i
t-ti
?l.i
r
:i
I I
' ,
i-
)•. r '
II
,11,,.l,*'!,
"«-„
i<ti
Three major factors of emplacement of
plutons in Uie mesozone are inferred to be
stoping or block foundering, crowding aside
of the walls, and uplift of Uic roof. The sideward
expansion may in part result in plastic flowage
of country rock upward and downward. Additional factors are incorporation of country
rock and metasomatism of wall rock. The
importance of each factor varies with the
particular example. If the tonalities of the
baUiolith of Southern California are inferred
to result from incorporation of gabbro by
granodiorite magnia then gabbroic material
may be inferred to be equivalent to about half
of the tonalite that forms 63 per cent of the
area now occupied by the batholith. This
would make the problem of emplacement of the
batholith one of how so large a volume of Uie
initial gabbro was introduced as wdl as of
how so great a mass ot granodiorite was cmplaced. Similariy at least 10 per cent of the
problem of emplacement of the Coast Range
batholith of Alaska and British Columbia
could be related to incorporation of mafic
rocks. Most of the mafic rocks in orogens, however, are lava flows and intrusive diabase,
dolerite, or gabbro sheets emplaced under
conditions of the epizone previous to major
deformations.
A great variety of structures associated wiUi
plutons ot the mesozone have been cited as
consistent v/ith formation by upward movement
of magma. Such structures within the plutons
are subvertical foliation and lineation in border
facies, marginal fissures wiUi pegmatite or
aplite, marginal upUirusts, radial dikes, and
schlieren domes; structures in the country rock
near the pluton may be increase in dip of
foliation or of slaty cleavage or of the plunge of
lineation, subvertical lineation and subvertical
secondary fold axes of plastic flowage origin,
"slip cleavage roughly similar in strike to the
periphery but dipping outward wilh the lower
schist layers moving up relative to the overlying layers, and development of domical
foliation in the roof.
Structures consistent with outward expansion effected by the pluton are deformation
of beds into partial conformity with the periphery, intensification of folding, and in part the
intensification of planar foliation in the border
fades of the pluton itself.
All discordant structures need not necessarily
mean stoping, for expansion effects of the
pluton may result in pulling portions of the
this possibility is not of suffident magnitude \ ^ " e a l cross section of batholiths in Uie
satisfy the actual rdationships.
W ^ ^ ^ ' P^^t of the mesozone with Uie areal
•w|oo55 section of their feeders from the catazone.
Emplacetttent of Plutons in Catazone
^
^^""^^ °f ^^^ '"^^"^'^'^ " ^ ^ ' "'""'^ ^^
seems to be a major kind in the catazone, and
often phacoliths. of both igneous and of metasomatic origin are reported to be associated.
Many .xenolithic domal batholiths may also.
li the writer has correcUy interpreted the
literature, then most, perhaps all, of the
plutons of the catazone were emplaced under
synkinematic conditions. The roof portions of 8
number of batholiths of the mesozone are
similar to those of plutons emplaced in the
catazone, but such conformable emplacement
in the mesozone does not, in part at least,
appear to be related necessarily to regional
tectonic forces. Such plutons may be inter-^'
mediate between tho.se typical of the mesozoncs
and those characteristic of the catazone. The
extent to which plutons of the catazone are
due to metasomatism or anatexis is yet to be
definitely determined. I t is logical to assume
that at their source granitic masses would as
a result of anatexis and rise of temperature
become mobile and rise as diapirs or as "migmamagma", but the extent to which source areas
are now exposed is most problematical.
Marshall and Narain (1954, p, 73) have post
^^^'
ulated tiiat the negative gravity anomalies over
ver.
• • •' •
granite batholiths, of a type here inferred to;
—ji"_^
w^w
ri-fz:-^
• '
'
* *
belong to the mesozone, are due to "granite
Conlormoble granile, Psuedo gronite
Gronite
roots", to extension of the granite pluton to j
Orthogneiss in
gneissoid lo gneissic
gneiss by
lectonoptoslic
depth, rather than due only to density congranitization
folds and domes
trasts between granite and country rock near
the present surface. Presumably this could
FIGURE 19.- SCItEMATIC S K E T a i S H O W I K G POSSIBLE S-rRUCTURAL RELATIONSHIPS OP PiUTONS
IN EPIZONE, MESOZONE, ANU CATAZONE
mean continuity of plutons of the mesozone
with those of Uie catazone, Biehler and Bonini J Question is left open as to whether batholiths of mesozone enlarge downward in continuity with
(1958) have conduded that, if reasonable, Itose of catazone or whether they have roots
assumptions are made for die probable geology
in part at least, result from a phacolithic
and density distribution of the region of the streamlined and comparable to the shape of
Boulder batholith, it follows that a granite salt diapirs with pinched-off roots. The, lower mechanism ot emplacement, usually igeneoiis
mass roughly with a plano-concave cross part of such bodies should have inward dips. but in part metasomatic.
Age determinations permit the inference
section and a depth not much less than and Symmetric funnel-shaped plutons such as the
that
the youngest plutons of the catazone with
Loon
Lake
(Fig.
14)
are
few,
but
a
number
of
not much more than 10 miles will closely satisfy
the residual negative bouguer anomaly. An ' liccp-seated plutons such as the Cheddar extensively developed migmatities are about
additional narrow root could also be presentj] batholith (Fig. 14) and the souUiwest side of a 100 ni,y. old and that plutons of the epizone
Grout (1945, p. 276-278) on the basis of !>art of Uie Coast Range baUiolith are asym- may be at least as old as 1.65 b.y. and probably
some experimental evidence suggests that large metric in cross section and bordered on one much older. Plutons of the mesozone range in
intrusives that rise from great depths may side by inward-dipping schists. The problem age from slighUy less Uian 100 m.y. to those of
have only roots or a series of roots and that ol batholithic roots in the transition zone the Keewatin belt ot Uie Canadian shield which
they' may ascend along part of their route between the mesozone and catazone and in are 2.5 b.y. or older.
because some of the overlying rocks become the catazone deserve more detailed study.
Origin of Granitic Magma
so reduced in viscosity that they move aside The details of Uie interrelations of plutons
o
f
the
catazone
to
those
of
the
mesozone
.and
"We must still entertain the hypothesis tItcU most
and down along the sides in a mobile contact
zone. There may be accompanying distention- ol those of the mesozone to those of the epizone granites have been produced tliroughoid geologic
and sideward flow in the roof during emplace- temain as problems. A tentative schematic time by diJIerenliation of basic {basallic) magma.
ment. Such a mechanism nf intrncinn ivnrilil rfiaprnm n f r p l j l l i n n c V i i n c ic c h n w n i n T ^ i o i t r p 10
The role of metasedimentary material as the
prime source of most granitic magma is now
emphasized far more than is implied in the
statement of Bowen cited above. There appears
to be a tendency at the present time to start
wiUi the assumption of at least two major
magmas—one, Uie granitic derived from the
sialic part of the crust, the other, the basaltic
(rom deeper down, probably in the manUe, or
beneath the continents from an eclogite root.
Graywacke forms a large part of eugeosyndinal sediments. It would with increasing
melting yield successively a litUe true granite
and then a Irondhjemitic magma. The latter by
reaction with associated basalts would result
in a tonaiitic magma. Partial melting of an
illitic type of clay has been shown by Winkler
(1957, p. 57-58) to yield an exceptionally
potassium-rich leucogranitic magma. The
hypoUiesis that the lowest part of the sial
contains some primordial granitic material
differentiated from basaltic magma however
is reasonable and has not as yet been precluded, especially for the early stages of geologic
history. Remdting of such primordial granite
would, of course, yield granite magma direcUy.
An andesitic magnia may form by partial
mdting of a gabbroic or cdogitic continental
substratum or essentially by incorporation of
graywacke in basaltic magma.
Basaltic magma maj' yield basalt or gabbro
dirccUy by consolidation; dioritic-andcsitic
magma by assimilation of sialic material or by
mixing of femic and salic magma; and ultramafic, anorthositic, monzonitic, granophyric,
and other subordinate facies by differentiation.
The granitic magma may yield granites direcUy; minor diorite by incorporation or
metasomatism of mafic rock; and mobile
quartz dioritic or other intermediate kinds of
magma by incorporation of graywacke and
eariier basalt flows or gabbro plutons. The
'quartz dioritic magmas may in turn yield
granodiorite, quartz monzonite, and new
granite magma by differentiation. The initial
volume of gabbro emplaced in Uie mesozone
and epizone must have been much larger than
that now represented by exjjosure. Much ot it
foundered in later intrusive granitic magma
and was incorporated to reappear in Uie modified facies sudi as quartz diorite.
Read (1951, p. 22) has made a tentative suggestion that "w6 seek Uie ultimate source of
the granitising fluids in crystallising simatic
material below the site of the gcosyndine."
Adoption of such a hypothesis has a number of
significant consequences. Simatic material in
crj'stallizing at depth slowly over a long time
may be expected to undergo fractional crystallization and differentiation to yield directly
magmatic monzonitic to dioritic differentiates
(especially if magnia is undcrsaturatcd) of
magmatic granitic differentiates (if oversaturated). The released granitizing fluids,
either magma, gas ions, or all three may !«
expected to modify the material in the lowest
part of the gecsyncline and add to or develop
granitic magma. The effect of pressure in
raising the temperature of mdting is not adequate to prevent a rise of temperature and
pneumalolylic fluids from fluxing granitic
material at the base of Uie sialic part of the
crust rather than higher up. The source zone
for the plutons would therefore not be expected
to be exposed.
TutUe (1955) has estimated that wilh a,
geothermal gradient of 30°C. per km partial,,
melting of a geosyndinal prism of sedinienU
might start to yield a biotilic granitic magma
with" a temperature of about 640°C. at a deplh
of 21 km and that complete melting with about
2 per cent HjO could occur at about 31 km.
WiUi a gradient of 40°C. per km incipient
melting could occur at a depth as shallow as
15 km.
The usual order of intrusion—gabbro, quartz
diorite, granodiorite, quartz monzonite, and
granite—in composite plutons is one that
corresponds to the order theoretically expectable as a result of magmatic differentiation!
or alternatively to that of decreasing temperatures. A speculative hypothesis lo explain this
order might be as follows. The early rise of
basaltic magma direcUy yields gabbro plutons,
diabase sheets, and Isasaltic lavas; basallic
magma wilh incorportation of sial leads Id
andesitic lavas and minor diorite plutons..
Subsidiary effects of the development and
rise of basaltic magma and its derivatives are
accentuation of the rise of the isogeoUierms and
fluxing in Uie lowest part of the sial. As the
isogeotherms rise through the deep sial early
formed interstitial low-melting granitic fluids
work upward, react with country rock in partj
and result in a differentiated domal column
ranging upward in composition from residual
refractory materials at the base through quarU
dioritic and granodioritic facies to granile alj
the top. Eventually the continued rise of the
isogeotherms results in suflicient melting of^
the lower portion of the column—either the:
quartz dioritic or granodioritic facies—so thalj
i rises as a whole followed successively by mesoperthite granite bulks large in the AdironMlting and rise of the overlying materials. dack belt of catazonal rocks.
Granodioritic magma may in turn react with
nafic material on its upward flow to yield
Problem of Volcanic and Plutonic
liiartz diorite. Later granitic magnia may
Associations
lisc through a sheath of the earlier intrusives.
One of the most critical problems is whether
Olher hypotheses are desirable.
The variation in ratio of different kinds of or not our present knowledge indicates, or is
ipieous rock in the different zones needs study. consistent with, the hypothesis that there is a
The plutons of the epizone may be predomi- direct relationship between salic volcanic rocks,
nantly granodiorite, quartz monzonite, and aphanitic or porphyritic intrusions, and
Jianile, The tonaiitic facies in general appear granitoid plutons.
Kennedy (Kennedy and Anderson, 1938)
to form a larger "percentage of the rocks in the
plutons of the mesozone Uian in those of the has made a sharp distinction between volcanic
q)izone. Quartz monzonite, granite, and and plulonic associations with respect to
leucogranite or alaskite are far more common igneous rocks. He postulates that the volcanic
imong the members of the granite family in associations include not only lava flows and
direcUy related vent intrusions but also such
tertain bdts of the catazone than in the
intrusions as the great sill swarms of the
mesozone (Daly, 1914, p. 60; Osborne, 1956).
Karroo, South Africa, the Palisades sill of NewIn particular, andesine-quartz diorite apJersey, and even the great sheets such as the
parently is rdatively subordinate in these
Bushveld igneous complex of the Central
belts. Andesine and labradorite anorthosite
Transvaal, South Africa, all of which are in
»nd gabbroic anorthosite of the types found in nonorogenic areas and intimately associated
inassifs and independent sheets are possibly wilh volcanic phenomena. Plutonic associations
•Imost exclusively in belts of the catazone. on the olher hand he suggests appear to be
•fuming Uie foregoing relationships arc" limited to orogenic regions and consist almost
correct, although wc do need quantitative data entirely of granodiorite and granile together
to substantiate them, some suggestions as lo with smaller amounts of their associated pretheir origin may be offered as bases for sludy. dominanUy homblendic, basic, ultrabasic, and
Is the restriction of the types of anorthosite lamprophyric types, while typical gabbros are
mentioned to the catazone the result of Uie characteristically rare or absent. He further
necessity for the kind of environment which by states that volcanic associations, on the conwting as a plastic envelope (the country, rock trary, are overwhelmingly basic and are comis often marble) under high pressure permits posed mainly of basaltic magma or of rock
the retention of the high volatile content es- types belonging to a basaltic line of descent.
antial to keep the equivalent magma fluid He condudes (1938, p. 30) Uiat
md of gabbroic anorthositic or anorthositic
composition, or is it a phenomenon to be corre- "Altogether, there does not appear to be any very
evidence to indicate a close connection belated wilh greater age, or-both? A favorable direct
tween plutonic activity and volcanicity"
bome for quartz diorite is the mesozone. Is
this because the quartz diorite magma origi- and (1948, p. 2-3) that
nates largely through reaction of more alkalic
granitic magmas with mafic rocks, thus losing "there is a universal absence of lavas belonging to a
contemporaneous with the rise of batholithic
lluidity and lo a substantial extent not rising period
intrusions to their highest levels in the crust."
ibove the mesozone? Is the predominance of
granodiorite and granite relative to quartz
A recent discussion of the problem has been
diorite in the epizone the consequences of given by Raguin (1957, p. 185-199). He refers
equivalent magmas being the lightest types to subvolcanic granile masses as truly very
ind fluid at relatively low magmatic lempera- special and exceptional and moreover amlures because of volatile content and their biguous in interpretation. He attributes to E.
lower melting intervals? Why the predominance Suess the development of the concepts that
ol granite in certain catazonal bells? One successively deeper denudated levels reveal
iinswer might be, "They are granitization lava flows, hypabyssal porpln-ry intrusions,
products". But the writer is not convinced and grained plutonic bodies of similar comthat this is the whole answer because magmatic position but different texture and that all are
M,..,.W>.1\.U1I >
,i.y n;iiuc(i. j-ic also presents a discus.sion of an opposite philosophy that envisages
the foregoing concepts as seductive but deceiving and that interprets the association of
volcanic rocks and major plutons in the earth's
crust to have no direct relationship. Some
proposed objections to the Suess concepts are
that the succession in plutonic rocks is from
basic to add but in volcanic rocks from acid
to basic, irregular or recurrent; volcanic rocks
may occur independent ot plutonic rocks, and
vice versa; volcanism is related to periods of
fracturing of the crust, plutonism to periods of
folding; plutonism occurs after vulcanism; a
true volcano has never been observed to rise
from a plutonic mass; and identities such as
volcanic and plutonic quartz porphyries are
only a phenomenon ot convergence, Raguin
concludes that the problem of the relationship
of vulcanism to plutonism is still unsolved.
The ideas of Kennedy have been criticized
by Tyrrdl (1955, p. 420) who writes
"The lava series ranging from pyroxene andesite to
rhyolite, therefore, has the same chemical composition, the same geological and geographical distribution, the same tectonic environment, and appears
at the same stage of the tectono-igneous cycle as
the plutonic series ranging from quartz diorite to
gran te. If the latter belongs to the plutonic association there seems to be no escape from Uie conclusion that the andesite-dacite rhyolite series likewise
does , , , . The writer suggests that the whole trouble
with plutonic and volcanic associations is that they
are wrongly named,"
The many citations (21) in this review demonstrate that it is normal for volcanic rocks of
equivalent composition to be associated in
space, time, and tectonics with plutons eraplaced in Uie epizone.' Many granitic bodies
that have been called plutonic because of their
medium to coarse grain and their batholithic
size are not plutons in the sense of deep-seated
emplacement. Exceptionally cogent examples
Uiat provide a dear demonstration of the succession of magmatic activity from volcanism
to high-level granite emplacement have been
described from Northern Nigeria by Jacobson, MacLeod, and Black (1958, p. 7). Here
are about 40 granite complexes in a belt about
270 miles long and up to 100 miles wide. The
total area of granite is about 2000 square
miles, and there is about 500 additional square
miles of rhyolite of similar chemiail composition and age. The rhyolite furthermore is
almost wholly confined within the granite
ring complexes. The granite plutons are up to
285 snuarc, milpc In •,.•''- tt ii
about 3 times as many complexes, ead) about 3 times the area, in the mesozone!
ncaUi this bdt, it would mean a contin*.
great batholith, 270 miles long wiUi an astnl
width of 65 miles.
Some of the very small plutons of the i,
may be granitic, granophyric, or monz
differentiates of basaltic magma bodies io.
somewhat below. But it seems essential _
most of the salic lava flows and stodcs and^
the baUioliths of Uie epizone originated
granitic magma of deep-seated origin.
A diversity of succession in lava sequo-.
can reasonably be interpreted in terms of am
cessive pulses of basaltic or andesitic m*
from depUis and magmas of Uie rhyc
rhyodadtc, dellenite, dadte group •'I
epizonal plutons. It is also probable thats.
of Uic epizonal dikes of granitic composti
came direcUy from great depth raUier ti_
from epizonal plutons. In summary, Uie iml^
rocks are predominanUy extruded as lavwV
emplaced in Uie epizone, whereas Uie fd
rocks, although induding lava flows and nsL
rdated plutons emplaced in the epizone, aicl
volume per cent largely emplaced i n i i
mesozone and catazone. If Uie granite o ^
nated as a differentiate of gabbroic magm*^
the mesozone or catazone, at a levd above*)'
source of the gabbroic magma itsdt, Uien bo<"
of gabbro at least 10 times as large a s |
granite plutons should be common-'inlmesozone or catazone of the orogensl4Sii
bodies do not occur in appropriate volu
Uiese zones as now exposed.
CONCLUSION
The foregoing survey shows that the autl
who have reported on detailed strudL
studies of stocks and batholiUis in No
America have reasoned that granitization (
occasionally has played a role in Uie mcduL
of emplacement of plutons in Uie epizone,!
been of subordinate significance (one uil^
excepted) in the mesozone, but has playo
major although not necessarily a greatJy*t
ponderanl part in the catazone. Otherwi*1
rdiance has been on magma empln.
One might also condude from such a ._
however, that the unity of agreement in i n t t ^
tation has been far too great to be heaJthjr I
the optimum advance of our undeist
Hypotheses, in general, as lo the
roles of magma and of metasomatism•'iO?
the problem remains one demanding
studies and more dependable criteria.
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U]
RISEAUCH INSTITUTE
EARTH SCIENCE LAB.
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Copyright 1974. All rights reservttt
REGIONAL GEOPHYSICS OF
THE BASIN AND RANGE PRO\aNCE
x 10021
George A. Thompson
Department of Geophysics, Stanford University, Stanford, California 94305
Dennis B. Burke
U.S. Geological Survey, Menlo Park.California 94025
Of late years the most important contributions have come from the Physicists,
and in their scales have been weighed the old theories of Geologists.
G. K. Gilbert (1874)
INTRODUCTION AND G E O L O G I C SETTING
Nearly one hundred years ago, Gilbert (23, 24) and other geologic pioneers
introduced the idea Ihal much of the seeming jumble of mountains and valleys
in western North America was the result of far different processes than fold
mountain systems such as the Appalachians or Alps. Afler a century of geologic
and geophysical investigations in the region, it is now generally accepted that the
physiography ofthe Basin and Range province (Figure 1) is one of sculptured and
partially buried fault-bounded blocks that have been produced by the extension of
the region during laie Cenozoic time. Crustal blocks composed of complexly
deformed, diverse pre-Cenozoic rocks and relatively undeformed, predominantly
nonmarine volcanic rocks of early and middle Cenozoic age have been variously
uplifted, tilted, and dropped along numerous normal faults throughout a broad
region from Mexico to Canada—from as far west as California and Oregon to as
far east as western Texas (e.g. Cook, 13; GiUuly, 27; Thompson, 76).
The distribution of late Cenozoic normal faults in the western United States is
shown on Figure 2 (note that the regional extent of faulting is somewhat larger
than the Basin and Range physiographic province of Figure 1). The recent
seismicity (Figure 3) shows that small earthquakes are widespread in what
Atwatcr (5) called a wide soft zone accommodating oblique divergence between
the Pacific and North American plates. The net effect of fault movements within
this region is a crustal extension oriented roughly WNW-ESE. The actual motion
on individual faults is quite variable, however, and appears to be conirolled by
the orientation of faults with respect to this principal extension (Thompson &
Burke, 78). In the northern portion of the region—across Nevada and western
213
,
,
214
THOMPSON & BURKE
6 V J .>. 'I
NEVADA
f
\I/2U\
.
f
.UTAH
\
WoA\
•
!
\\%)
\
% \ +
OJLORADO
.S^LIFORNIA^ V X ^ ^ ^
13J"
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\vt
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1
''TXr^^
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S
joo
.\
r
lie*
.-»
^^
_I16«
I 114" \
T
,
1
\
*Ow,^r, I
11}°
IIOC
\
J
+
108'
.
1
•••
jH—'x
\0t,°
VilOili::^
Figure 1 Physiographic provinces ofthe western United Slates (Fenneman, 21).
Utah—the domain of faulting is neatly confined between the Sierra Nevada of
California and the Wasatch Mountains of north-central Utah. The relatively
unfaulted Colorado Plateau separates the central portion from a zone of faulting
in the Rio Grande trough in New Mexico and west Texas. Relative motion between
Ihe unexiended and rather enigmatic mass oflhe plateau and the encircling faulted
terrain is presumably accommodated by a compoiienl of right-laieral strike-slip
along Ihe southern plateau border. Faulted terrain extends southwards without
interruption into Mexico and the Gulf of California. Faulting seems to die out to
Ihe norlh, and the manner in which relative motions are accommodated along
the northern boundary remains a troublesome problem.
REGIONAL GEOPHYSICS OF THE BASIN AND RANGE PROVINCE
'S*..
215
,^-
IT)—\-^
—I
* I ^' Kv + + *
'
T-^-v- L , > j ^ ^ -
*
—1
+ /
I —
«•+
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s \
4-.—\'i
11/"
ii}°
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108°
+
'
106°
\
*•
*
'-104°
;
-^
r^^
Figure 2 Predominanily normal (Basin and Range) faulis of late Cenozoic age in the
western United States (modified from Gilluly, 26).
Although the Basin and Range province is in many ways a unique physiographic
and geologic entity, increasingly precise and reliable geophysical studies, logeiher
wilh advances in tectonic theory, highlight similarities between the province and
other regions of pasl or present crustal extension. Il has a high heat flow and
widespread volcanism like other regions of active normal faulting, such as the Rifi
Valleys of Africa, the Lake Baikal depression of ihe USSR, Ihe Rhine graben of
Europe, Ihe marginal basins of the western Pacific Ocean, and the worldwide
system of oceanic ridges and rises. Along wilh Ihe Sierra Nevada and Colorado
Plateau, it forms a wide elevated region averaging 1-2 km above sea level and thus
may resemble the elevated, thermally expanded oceanic ridges (Sclater &
216
THOMPSON & BURKE
'
. -, k^--—--,.^-1.•^ /; ^ * +
1
+
+
+
1
* ' *
^
" * - - • — *
.—-
1
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; + . - . * • • +
-t-
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-1-
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-J
+ •'
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w
*°-
S I
^'"^
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ir"-
\7f
••
I
\
100 TOO
+
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KM.
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1—1
$?•••"
(
0
„ •
HO*
118°
iA»
l'v<';.^'
n?°
!
I
I
l-I
110°
-t-
+
v^
ioa°
*
^ 104'
f
Figure 3 Earthquake epicenters in western North America for the period I96I-1970.
Small dots represent earthquakes of magnitude about 3 to S, large dois greater than S.
National Oceanographic and Atmospheric Adminisiralion epicenlers replolted by J. C.
Lahr and P. R. Slevenson oflhe US Geological Survey (personal communication, 1973).
Francheteau, 65). Also like some of these other regions, il has a thin crust and low
manlle velocity.
Can regional geophysical data for Ihe Basin and Range province, combined with
interpretations of its geologic history, lead toward a better understanding of ihc
lecionic processes Ihat have controlled its development? To what extent have
earlier geologic events in the region preordained the pattern of faulting that we now
sec in western North America? What constraints must be heeded in tectonic models
oflhe region, and what aspects oflhe province allow these models to be compared
wilh olher portions of the global syslem of ever-changing Hthosphere plates? We
RKGIONAI. CEOPHVSirS OF TIIE BASIN AND RANGE PKOVINrE
217
believe Ihis last consideration to be of great importance, although it can only be
touched on lightly here, because much understanding of Ihe province derives from
analogy wilh olher regions of crustal extension. The currently most promising
models relate Basin and Range structure lo an earlier subducting plate al the
western margin of Norlh America, and they incorporate close physical comparisons
wilh the marginal basins ofthe western Pacific.
REGIONAL CRUST A N D MANTLE STRUCTURE
Crustal Thickness: Seisniic Refraction
Seisniic waves from explosions have provided Ihe most r£liable and detailed
information on crustal thickness and indicate Ihal Ihe region of distinctive Basin
and Range structures corresponds quile closely with a region of Ihin continental
crust (Pakiser, 52; Prodehl, 55). Prior to Ihe work of Tatel & Tuve (74) il was
generally assumed Ihat Ihe crust would be thicker under Ihis elevated region than
in conlinenlal regions near sea level, a relationship that has been found in other
mountain regions. It was thought that lateral variations of velocity and density in
the manlle were unimportant, or at least inconvenient in seismic inlerpretation, and
that isostatic compensation was accomplished mainly by varialions in crustal
thickness.
Talel and Tuve found thai the crusi in northwestern Utah is an anomalously
Ihin 29 km. Verification came from Berg el al (6), Diment el al (16), and Press (54),
although ihese authors initially used a different definition of the crust. They found
abnormally low P-wave velocities of 7.6 lo 7.8 km/sec al shallow deplh for what
we have now come to identify as P„, Ihe wave traveling in Ihe uppermost manlle
below Ihe M discontinuity.
Extensive explosion studies carried oul by Ihe US Geological Survey established
the basic picture as we know it today. David H. Warren, of Ihe USGS (persona!
communicaiion, 1973) has compiled and interpreted these and olher data into a
contour map of crustal thickness (Figure 4). The contours are based on data of
varying quality and on varying interpretation of velocity structures within the crust;
nonetheless they represent a good first approximation. Almost Ihe whole region
from Ihe Rocky Mouniains westward has a thin but variable crusi, roughly iwo
thirds the thickness found in slable regions of comparable elevations. The eastern
border oflhe Basin and Range province is marked by a fairly sharp gradient al Ihe
35 km contour lo a thicker crusi under the Colorado Plateau. Southeast of ihe
Colorado Plateau there is some indication of thinning beneath the Rio Grande
trough of New Mexico and west Texas.
The crust is thicker beneath the Sierra Nevada to the west of the province
[although this conclusion has been called into question by Carder (10)]. Il is
interesting lo point oul that in detail the thick crusi of Ihe Sierran region (Figure 5)
extends into the Basin and Range province to the east of Ihe Sierra Nevada. TTie
eastward extent of thick crust does nol correspond with ihe eastern border of the
Mesozoic Sierra Nevada batholith (Figure 6), however; although a correlation of
Ihe low velocity zone with the border of ihe balholith is not ruled oul.
218
THOMPSON & BURKE
J6
+
>6 /
/•*
+
*'
44+ «
51+48 » * « 48t
J
51
-t^
I
Figure 4 Contour map of crustal thickness (in kilometers) based on seismic refraction
studies. Small numbers indicate individual thickness determinations. Compiled by David
H. Warren from Ihc following sources: 1, 4, 7, 11, 16. 19, 20, 22, 30. 34-39, 44, 55. 57-59,
62, 66. 67. 70. 72, 73, 82-85.
Upper M a n t l e Velocity and Implications From Gravity
When il was found Ihal the crust is abnormally ihin beneath the Basin and Range
province and adjacent regions il was also discovered that P„ is anomalous, lis
velocity of 7.7 to 7.9 km/sec is significantly less than Ihe normal velocity of about
8.2 km/sec observed in stable regions (Pakiser, 52; Herrin & Taggart, 33; see
Figure 7), Most of the Basin and Range province is characterized by the lowest
P, velocities, less than 7.8 km/sec.
REGIONAL GEOPHYSICS OF T H E BASIN A N D RANGE PROVINCE
COAST RANGES
CWATVAlUY
219
SIERRA NEVAOA
KASIN AND RANGE PROVINCE
,.tUIUMOf
Figure 5 Crust and upper mantle structure in a section across central California and
west-central Nevada as deduced from seismic-refraction siudies. An allern-alive model
beneath the Coasl Ranges and Great Valley is shown by dashed lines; topography
greatly vertically exaggerated (from Ealon, 20).
Gravity data supply a fundamental constraint on the amount of mass per unit
area underlying any region. This information is particularly valuable because
seismic refraction measurements do not by themselves allow inlerpreialions of ihe
thickness of the anomalous upper mantle of low P, velocity. Gravity interpretation
utilizes: 1. crustal thicknesses from seismic refraction, 2. crustal densities estimated
from-seismic velociiies and geology, and 3. upper mantle densities estimated from
P„ velocities. The gravity dala then yield estimates of Ihe thickness of anomalous
mantle relative to stable regions (Thompson & Talwani, 79). The required thickness
of low-density, low-velocity anomalous upper mantle is at least 20 km over much of
Ihe region.
In comparison wilh stable conlinenlal regions near sea level, most oflhe isoslatic
support for the high Basin-Range and adjacent regions is in ihe anomalous upper
manlle. This material must surely be a key element in any tectonic model.
Isostatic gravity anomalies in the United Stales (Figure 8) show thai most of the
region from the west coast to the eastern limit of the Basin and Range province is
deficient in mass, wilh an average anomaly of perhaps around — 10 mgal. In this
respect the region is similar to marginal basins of the western Pacific, which also
tend lo be isostatically negative.
The Lake Bonneville Experiment
A natural experiment in graviiaiional unloading of the Basin-Range crust occurred
as pluvial Lake Bonneville, of laie Pleistocene age, dried up, leaving the Great Salt
Lake as its principal remnant. Prominent shorelines around the edge and on former
islands mark the successively lower levels of Lake Bonneville. TTiese shorelines are
domed up toward Ihe center as much as 64 m as a result of Ihe unloading (Gilbert,
25; Crittenden, 14).
220
THOMPSON A BURKE
iTTo:
•T
I I
! \
V.
^ ^1
APPROXIMATE LIMITS Of THE
SIERRA NEVADA BATHOUTH
s}-^-^
40°-
.._,
I'L
I"
•
" •.
^
.K^'t'l'r--
'i
'.
— i ' —
i
'
38°-.
100
I
0
30°-
133°
.1
?00
I 'I
'
+
•*-
-t-
JiT
wo ?00
KM.
H0°
HB°
16°
I
\
1
V.
»4° \
I
113°
1
Wtf
I
108°
I
106°
-*•
1 +
^104°
r-^
">
I
Figure 6 Distribution of granitic rocks in California and Nevada. Solid lines represent
major active strike-slip faults (from Crowder et al, 15).
Using data from this nalural experiment and a simple model of an elastic
lilhosphere Boating on a fluid asthenosphere, Walcolt (81) has computed the
apparent flexural rigidity of ihe lilhosphere and compared il with Ihat of other
regions subjected lo various kinds of loading and unloading. Walcotl's results, as
shown in Table 1, illustrate Ihal Ihe flexural rigidity of the Basin and Range
lilhosphere is unusually low. He suggests that ihe anomaly may be explained by a
"very Ihin lilhosphere, only about 20 km thick, wilh hot, lower crustal material"
acting as part of the asthenosphere. In contrast, the flexural rigidity of stable
conlinenlal and oceanic regions suggests lilhosphere thicknesses of 110 km and
REGIONAL GEOPHYSICS OF THE BASIN AND RANGE PROVINCE
Table I
221
Apparent flexural rigidity-of the lithosphere (from Walcott, 81)
Daia
Region
Apparent
flexural rigidity,
Newto«vmeters
Lake Bonneville
Caritiou Mountains
Interior Plains
Boolhia uplift
Lake Algonquin
Lake Agassiz
Hawaiian archipelago
Island arcs
Basin and Range province
Stable continental platform
Stable continental platform
Stable conlinenlal platform
Stable continental platform
Stable continental platform
Oceanic lilhosphere
Oceanic lilhosphere
5x10"
3x10"
4x10"
7 X 10"
6x10"
9x10"
2x10"
2x10"
Characierislic
lime, years
10*
5x10'
5x10'
5x10'
10'
10'
10'
to'
75 km or more, respectively. The low P„ velocity and high heal flow (discussed in
a later section) are consistent wilh Walcolt's interpretation.
Anomalous Mantle and the Low-Velocity Zone
Several studies have indicated Ihat Ihe Basin-Range region has an unusually welldeveloped upper mantle low-velocity zone (LVZ) for both P- and S-waves. The
relationship is not always clear between the accentuated LVZ (as defined by waves
refracted al deeper levels in the mantle) and Ihe anomalous upfjer mantle (as defined
by low P , velocity). In a sludy applicable to the central part of the Basin and Range
province in Nevada and western Utah, Archambeau and associates (2) derived a
model (Figure 9) in which the M discontinuity is at a deplh of 28 km and ihe /*,
velocity just below it is 7.7 km/sec. This low velocity remains nearly constant to a
deplh of 130 km, where it undergoes a rapid transition to 8.3 km/sec. Thus the
LVZ is about 100 km thick; it begins al Ihe top of Ihe mantle and coincides wilh
Ihe anomalous upper manlle.
In comparison, the same investigators derived three models applicable to regions
northeast and east of Ihe Basin and Range province, including the Colorado
Plateau (Figure 9). These models have in common a "lid" of higher velocity material
(P, about 8.0 km/sec) above the LVZ, which is only about half as thick as in the
Basin-Range model.
In the foregoing discussion a single model has been assumed lo represent Ihe
Colorado Plateau, and this assumption seems reasonable because of Ihe geological
uniformity of Ihe Plateau. However, within the limited resolution of Ihe data, P ,
velocities (Figure 7) appear to vary markedly over Ihe Plateau and would nol
allow a single upper mantle model. This seeming conflict invites further research.
Helmberger (31) developed a new technique for studying regional variations of
the LVZ. The method makes use of the nearly constant velocity of the PL wave in
the crusial wave guide and the regional variation in Ihe velocity of long-period
P-waves. Results are mapped on Figure 10 (York & Helmberger, 87) as observed
time differences minus Ihe time diflerence predicted from a model LVZ roughly
222
THOUPSON & BURICE
<»*.^
MUES
100
0
0
30°-
100
KM.
'
'
ur
i?C
'
na'
\
\
iw'
\ iu°
<
\
I
\
iii'
.-
I
iio^
1
ioa°
^
iw'
n
•
^ta*'
Figure 7 Contour map of P, (upper mantle) velocities (in kilometers per .second) (from
Herrin, 32).
comparable to the Colorado Plateau model of Figure 9. Progressively ifiore
negative At values (delays of the long-period P-wave relative to the model)
represent progressively thicker LVZ or lower upper mantle velocity. Positive values
represent thinner or higher velocity LVZ relative to the model. Two main zones of
ihick LVZ wilhin the - 3 sec contour Irend northward through easlern Nevada and
wesiern Utah and northeastward into the Rio Grande trough in New Mexico.
These zones join lo the southwest and con lin is e across southern California and
norlhern Mexico toward the conlinenlal borderland off soulhem California
(generally considered to have Basin-Range structure) and the Gulf of California. The
Colorado Plateau is strikingly outlined by the zero contour, which is expected
because the reference model resembles the Colorado Plateau mantle.
REGIONAL GEOPHYSICS OF THE BASIN AND RANGE PROVINCE
MUES
'
0
100
700
'—I'l I I'l—'
+
0
133^
100 300
130*
118°
\
.,
\
\
1
T
116°
,•!
"^.K.-^"~•«-.^ -h
+
\ 114* \
IKT
fN_,
~--^^
II?*
_j^J^
223
X
108*
106°
^*Uj^\
Figure 8 Regional isostalic gravity anomaly (based on Airy-Heiskanen concept with
standard column 30 km). Line pattern, greater than -I-10 mgal; slipplftd paiiern more
negative than - 10 mgal (from Woollard, 86).
In olher important investigations Robinson & Kovach (56) studied upper
manlle S-waves in the Basin and Range.province, and Herrin (32) compared Ihe
Basin and Range upper mantle wilh that of a stable region, the Canadian Shield.
Using direct measurements of Ihe travel lime gradient, Robinson and Kovach
found a thin lid zone (9 km) of shear velocity 4.5 km/sec at Ihe top of the mantle,
overlying a low velocity zone wilh a minimum velocity at 100 km. Herrin's
comparative model for Ihe Canadian Shield contains no LVZ for P-waves and only
a weak one for S-waves. The comparison is important because il emphasizes a
degree of similariiy between the Basin and Range and Colorado Plateau mantles
relative lo Ihe slable region.
224
THOMPSON &. BURKE
COIORADO
PLATEAU
BASIN AND RANGE
PROVINCE ^
pO—
6.7
7.7
-
~M
l O W VELOCITY ZONE
7J
~lt»
piso
-
NO«»AAl MANTLE
l-
—0-
-
CRUST
7.7
7.9
8.3
_
CRUST
6.7
8.0
M
iiDioNe
RP
7.7
7.7
78
79
B.0
B.3
i
LOW VELOCITY 70M6
IDO
ISONORMAL MANTLE
L
Figure 9 Generalized comparison of crusi and upper mantle structure in the Basin and
Range province -and Colorado Ptaicau. P-wave velocities are in kilomclets per second
(adapted from Archamlieau e> al, 2).
RATE AND DIRECTIGN O F SPREADING
Seismologicat Evidence
Recent studies of focal mechanisms of many small earthquakes highlight a
strikingly consistent direction of ongoing Basin and Range extension. Although
recent earthquakes have been concenirated near the eastern and western borders of
the province and in a belt across southern Utah and Nevada, evidence of older
faulting indicaies ihat they are a reasonable sample of this longer but much more
widespread lecionic activity.
Focal solutions compiled by Scholz et a! (64) show predorriinantly normal
faulting, with the extension direction ranging approximately from east-west to
northwest-southeast. The few examples of strike-slip motion are also consistent
with this extension direction.
Only a few of the larger historical earthquakes were accompariifid by surface
ruptures large enough for the amount of offset to be directly observed, and ihese
larger shocks (Figure 11) probably account for most ofthe total deformation. The
main norih-souih zone of historical faulting in Nevada and adjacent California iS
nearly conlinuous. Horizontal extension across the faults ranges from a few centimeters io a few meters (Thompson, 75) and is greatest near the norlh and south
ends of ibe zone. This wide range in extension, plus the existence of unfaulted gaps,
shows ihal the ICO-yr historical period is too short for measuring a meaningful rale
of extension.
Dixie Vailey, a Type Basin
Near the northern end of ihe zone of historical faulting, at the site of the 1954
faulting in Dixie Valley (Figure )2), two measures onong-term displacement have
REGIONAL GEOPHYSICS OF THE BASIN A N D RANGE PROVINCE
225
34°_
M°-
30°-
13J°
120°
lia
1
V
114° \
I
10°
I
110°
I
0
WB*
,
106°
1 +
^104*
>-*
/
Figure 10 Relative development of upper mantle LVZ (low velocity zone), expressed as
contours of time difference in seconds with respect lo a model LVZ similar lo that of
Colorado Plateau. Stipple pattern accentuates region of pronounced (thicker or lower
velocity) LVZ (from York & Helmberger. 87).
been investigated (Thompson & Burke, 78): 1. Displacements of the shoreline of a
late Pleistocene lake supply a measure of extension during the last 12,(XX) years
(Figure 13), and 2. fault displacements determined from geophysical exploration of
the valley give the total amount of extension for laie Cenozoic lime, at least 5 km
in 15 m.y. TTie average spreading rates are 1 mm/yr for the short interval and al
least 0.4 mm/yr for the total displacement. The spreading direclion we obtained
from large slickenside grooves on fault planes is approximaiely N55°W-S55°E,
226
fflOMPSON
& BURKE
«•.
+
+ Ii -^
1
'—.v.-.t
i—i.. +
-J
.+
V,
1+
+
+
-t-
+
+ oWi+
+
*
„1TO
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.__.—^-
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;1. 4 - \ J
i
I
'
'KU
I
<
. l«4'ft
tru
J-
+
I
T
,.
i'
1
t
.186«
\
It",
MILES
100
MO
I ' l I I ' I -»
0
100 300
KM.
W-
IST"
I
J
+.
•-•^
I
II}'
J.-!
1
I
I
"^ -I-
!10°
WIP
lOt"
^104'
, j ^
/
Figure SI Historic surface offseis and epicenters for earlhquakes of greaier Ihan about
magnitude 7 in the western United Slates [from Ryall et al, 61).
which corresponds well with ihe range of directions obtained from earthquake focal
mechanisms.
Dixie Valley is the only basin for which this much daia is available. A "simple
exlrapqlation to 20 major basins across this part of the province suggests a total
Basin-Range spreading of aboui 100 km (10% increase in crustal area) and a
spreading rate of 8 mm/yr. On somewhat difTerenl assumptions, Gilluly (28)
esiimaied that ihe area! expansion ranges from 4% to 12% oyer most of the
proving. S'iewart (71) estimated 50 to 100 km (5% to J0%) of extension on the.
basis of a careful analysis of all available data. Hamillon & Myers (29) suggesi
Ihal the extension may be as great as 300 kra (30%). More subsurface data on
many basins is needed lo improve these estimates.
227
REGIONAL GEOPHYSICS OH THE BASIN A N D RANGE PROVINCE
11
( 1 I R^"*^
1 b c M aknia
I / . .n<fa(»Ui:ikn.li>»
11
% ^ \
JMnoncbvlrad
r--''^^fy ^^-JM*" Y
jV.../
3it>6'-\/^
JA//
JV^ X
w/'-yiy
ff
jj^rt^iitai
"^^W^
y/
J /
[III
V
tl y
^
funJj
-V0
*00M
0
1300 rr
13
Figure 13 (above) Map of olfsel lake
shorelines in west-central Dixie Valley.
The relative verlical spacing of beach
ridges around the valley demoiislrales ihal
the highest beach ridge preserved in this
area (3544 ft) marks—like the tufa
cemented lerrace deposits on bedrock —
the highest lake stand. The age of the
high shoreline is 12.000 years (from
Thonip.son & Burke. 78).
Figure 12 (left) Dixie Valley region. Fault scarps formed or reactivated in 1903, 1915,
and 1954 are shown (from Thompson & Burke, 78).
L o a t s and Time of Basin-Range Faulting
T h e present seismicity (Figure 3) is a misleading guide to even Ihe geologically
youngest faulting. Fault scarps of Q u a t e r n a r y age are widespread and bear little
228
THOMPSON & BURKE
relation lo the seismicity. Slemmons (69) has documented this fact for Nevada wilh
maps of faults in three age groups covering roughly Ihe last 100,000 years. The
locus of faulting appears to have shifted randomly over the whole breadth of the
province rather than having been confined lo Ihe area of recent seismic activity.
Although older normal faults are known (Burke & McKee, 9), Ihe main onset of
block faulting is marked by the widespread disruption of drainage and formation of
local sedimentary basins about middle or late Miocene lime. The lower Miocene
ash-flow sheets which cover broad areas were deposited on surfaces of low tectonic
relief (McKee, 46; Noble, 50). The inception of Basin-Range faulting over al least
Nevada and adjacent California is dated al 15 lo 17 my. (see Noble, 50, for
references). It must be emphasized that after faulting began il was probably
sporadic in any one area. On physiographic evidence, some areas appear to have
been inactive for a long lime (for example, parts of Ari'zona, New Mexico, and west
Texas), while activity continued to Ihe present in olher areas.
THE PATTERN O F RUPTURE
Basin-Range faults are often described in a general way as high-angle normal faults
striking norlh lo northeast, but the impression conveyed by that description is
highly misleading. Individual faults lend lo be extremely crooked in map plan and
ihe fault pallern is more nearly rhomboid or even rectilinear. Some mountain
ranges are bounded by en echelon faulis that strike diagonal lo Ihe range (eastern
front of Sierra Nevada for example). Considerable warping and tilling ofthe blocks
accompany the faulting, particularly near the ends of elongate basins.
Nowhere is the fault paliern better exhibited than in Ihe late Cenozoic basalt
flows of south-cenlral Oregon (Figure 14), but similar patterns are common from
Nevada (Figures 12 and 13) lo Texas. Moreover, the roughly rhomboid map
pallern of faulting is characteristic of olher regions of present or past crustal
extension, such as the African Rifts, Ihe Rhine graben, the Oslo graben, and the
Triassic basins of eastern North America.
No well-founded explanation for Ihe complex rupture pallern is known.
Alternative hypotheses include changes in the stress system with lime, influence of
older structures, and anisotropy in mechanical properties of Ihe crusi. Another
possibility is that Ihe pallern is roughly analogous lo the near-orthogonal paiiem
formed by oceanic ridges and transform faults, a pallern which has been explained
as offering minimum resistance lo plate separation (Lachenbruch & Thompson,
42). Oldenburg & Brune (51) dramatically reproduced Ihe near-orthogonal oceanic
pattern in a laboratory model wilh a Ihin crusi of wax forming on molten wax, and
Duffield (18)observed similar patterns forming on Ihe solidified crust of a convecling
lava lake.
The simple application ofthe minimum resistance theory to Ihe Basin and Range
province would suggesi a series of noriheasi-lrending grabens (normal to Ihe
spreading direclion) and norlhwesl-lrending transform faults. The actual mechanics
arc more complex, and the faults commonly are hybrid, having components of
REGIONAL GEOPHYSICS OF THE BASIN AND RANGE PROVINCE
229
Figure 14 Rhomboid pallern of rupture expressed by laie Ceno-/oic normal faulis in
south-central Oregon. B^rbs on downthrown side of faults; faults dashed where inferred
(from southeast portion of plate 3 of Donath, 17).
both dip- and strike-slip. The pattern is nol simple and Ihe question of the
rupture pallern is far from resolved.
In addilion to the problem of Ihe pallern of faulting, the question of whether
the normal faults systematically flatten with deplh has been much debated, in pari
because such changes would imply greater regional extension. The seismic focal
mechanisms lend no supporl lo Ihe notion of major decreases in dip, however, and
serious geometric problems would ensue at ihe ends of basins if such decreases did
occur. Therefore the low dipping to subhorizontal normal faults thai have been
observed in surface exposures and mine workings seem best ascribed lo gravitational
sliding and tilting in response lo deeper primary faulting. The problem has been
explored by Stewart (71) and Moore (48). Armstrong (3) interprets low-angle fiiiilts
in eastern Nevada as gravitational sliding features of laie Cenozoic age.
HEAT FLOW A N D CRUSTAL TEMPERATURE
Regional Variation of H e a t Flow
A region of anomalously high heat flow comprises Ihe entire Basin and Range
province and extends across Ihe Columbia Plateau and part of the Rocky
Mountain province (Figure 15). Heal flow values greaier Ihan 2 HFU [heal flow
230
THOMPSON A BURKE
<W*-
/ ^\ \\
4 //
4?*-
,OA
AV -.4/,'. ,'L
A
Miics
3J°A
0
30*-
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•
9--20^
I^
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.i^l
^ L<r.Bx
100 200
IM^
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118°
IIB°
,w
O 116',.\
'«•.
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110°
Figure IS Contour map of heat flow. Contours in Heal Flow Units (/ical cm"' sec"');
dashed where extended on the basis of meager daia. Daia points shown as open
triangles are measured heat flows in the range 0 to 0.99; solid triangles, 1.0 lo 1.49; open
squares, 1.5 lo 1.99; solid squares, 2.0 lo 2.49; open circles, 2.5 to 2.99; solid circles, 3.0
and larger (from Roy el al, 60).
units (HFU), /ical cm"^ s e c ' ' ] characterize Ihis broad region, in contrast to
normal average values ofabout 1.5 HFU.
Although Ihe Colorado Plateau is al leasl partly an area of normal heat flow,
the distribution of measurements is inadequate to explore its boundaries with Ihe
Basin and Range province. The boundary wilh the Sierra Nevada appears to be
surprisingly sharp.
Another compilation of the regional heat flow, by Sass and associates (63),
231
REGIONAL GEOPHYSICS OF THE BASIN AND RANGE PROVINCE
—
CLAN ALPINE MOUNTAINS
DIXIE VALLEY
STIllWATER RANGE
1—
--..r;;
EA l e v t i
1
M
— *iii::::;::;
' • - • • • • • • •
-PT—^^£=^^^
• • "
W/7
-
\
\ \
\ W^A
^/y
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1
1
1
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4
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8
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•
Figure 16 Cross section of Dixie Valley, Nevada. The subsurface structure lo Ihe depth
of the sedimentary fill (stipjiled) is based on geophysical exploration. Dike al depth is
hypothesized to accommodate surface extension, as shown by arrows (based on Burke, 8;
Thompson, 76).
although more conservatively contoured, contains important additional details.
One cluster of consistently high values (mostly above 3 HFU), the "Bailie
Mountain high" in northern Nevada, is inlerpreled as a transient effect of fairly
recent crustal intrusion. To the south in Nevada, a cluster of values less Ihan 1.5
HFU, Ihe "Eureka low," is ihoughi lo be the result of unusual deep circulation of
ground waler. TTiese examples emphasize the importance of nonconductive heal
transfer. We point out thai spreading of the grabens may be accompanied by
intrusion of dikes at depths of a few kilometers (Thompson, 76), and these
intrusions may be imporiant in the heal transfer (Figure 16). The Battle Mountain
high is on Ihe projection of Ihe active zone of spreading (historic faull breaks) at
its north end (Figure 11).
The thermal transition to Ihe Sierra Nevada may occur within a lateral distance
of only 10 or 20 km (Sass et al, 63). If Ihis proves lo be the case, it will require
shallow heat sources and will strengthen the hypothesis of intrusions beneath the
grabens. Furthermore, present evidence suggests that the heal flow boundary with
Ihe Sierra Nevada follows in detail Ihe irregular boundary of the normal faulting
and nol Ihe generalized physiographic or topographic boundary.
Heat Production and the Linear Heat Flow Relation
A surprising and remarkably simple relationship has been found between heal flow
and the heat production of surface rocks in plutonic areas; that is, within areas
such as the Sierra Nevada and Basin and Range province, ihe heat flow varies
232
THOMPSON & BURKE
linearly with the radioactive heat production al the surface (Roy et al, 60). This
relationship is best explained by an exponential decrease of heat production with
depth in the crust, combined with an additional flow of heat from the mantle
(Lachenbruch, 41). The flow from Ihe manlle—called Ihe reduced heal flowamounts to 1.4+0.2 HFU in the Basin and Range province, compared lo 0.8±0.1
HFU in Ihe United Slates east oflhe Rocky Mountains and only 0.4 HFU in the
Sierra Nevada (Roy el al, 60).
Crustal lemperature profiles for ihe three heat-flow provinces have been
calculated by Lachenbruch (41), based on Ihe exponential model. Temperatures al
a deplh of 30 km in the Basin and Range province range from 7(X)-1(X)0°C
(depending on surface heat flow or heal production), as compared lo 400-600°C in
eastern United States. Temperatures in the Basin-Range crust may thus reach the
melting range for granite, and temperatures in Ihe upper manlle may reach melting
for basalt. These high temperatures, combined with widespread laie Cenozoic
volcanism, form a basis for Ihe generally accepted hypothesis ihat partial melting
is responsible for the thin lilhosphere and for Ihe shallow, accentuated low
velocity zone (asthenosphere) of the Basin and Range province.
TTie conductive model will need lo be modified if much heal is carried into the
crust by intrusions beneath spreading centers, as we have suggested (Figure 16).
Hot-spots and Mantle Plumes?
The Vellowslone volcanic region in northwestern Wyoming may represent a hol-spoi
above an upwelling convective plume in ihe manlle (Morgan, 49). According lo
Morgan's theory Ihe Norlh American lithosphere as a whole is moving weslsoulhwesl with respect lo the mantle. The trail of the persistent Vellowslone
hoi-spol across its manlle plume would be marked by the older volcanics weslsoulhwest of Yellowstone (in the Snake River part of the Columbia Plateau
province). Other possible hol-spots have been suggested within the Basin and Range
province.
A significant point about Ihe theory should be kept in mind regarding ihe origin
oflhe fault-block structures. If the Vellowslone plume is a driving mechanism for
Ihe structures and Ihe lilhosphere is moving westward across it, the locus of BasinRange tectonic activity should be migrating eastward; and we know of no strong
evidence for an eastward march of tectonic activity. Westward movement of Ihe
lithosphere at a rate on the order of I cin/yr would have produced a movement of
150 km in Ihe 15 m.y. since the inception of Basin-Range faulting.
MAGNETIC AND ELECTRICAL ANOMALIES
Anomalies in Ihe regional magnetic field and in eleclrical conductivity generally
supporl other evidence of a hoi upper mantle in the Basin and Range province,
but the resolution of lateral varialions has so far been very limited.
Zielz (88) showed Ihal from the Sierra Nevada lo ihe Rocky Mountains, magnetic
anomalies are subdued in amplitude, and Ihal long-wavelenglh anomalies are
REGIONAL GEOPHYSICS OF THE BASIN AND RANGE PROVINCE
233
absent This fact suggests that the lower crust and manlle may be above Ihe Curie
temperature (578° for magnetite). Surprisingly, the magneticfieldover Ihe Cojorudo
Plateau does nol appear to differ significantly from Ihal over Ihe Basin and Range
province, in contrast lo results from other kinds of siudies.
Porath & Cough (53) explored varialions in manlle eleclrical conductivity from
Ihe eastern and southern Basin and Range province lo the Great Plains by
measuring geomagnetic fluctuations. The anomalies are well represented by
varialions in depth lo a half-space of conductivity 0.2 (ohm m)"'. The lop of this
conductor is inferred lo correspond approximately wilh the I5(X)° isotherm. Depths
lo the surface of the conductor are 190 km under the Basin and Range province
and 350 km under the Colorado Plaleau, wilh a ridge of depth 120 km al Ihe
boundary. The deplh under Ihe Rio Grande trough is 120 km, ihal under ihe
soulhem Rocky Mouniains is 150 km, and thai under Ihe Greal Plains is 350 km.
Although such models are naturally nol unique, they strengthen the interpretations
of regional heai-flow varialions and add anolher dimension lo ihe unusual
properties of the Basin and Range province.
PETROLOGIC RELATIONS
Three imporiant relationships among Ihe rocks deserve special emphasis:
1. Prior to Basin and Range faulting, lower and middle Cenozoic volcanoes
erupted largely intermediate-composition rocks that become more alkalic toward
ihe conlinenlal interior (Lipman el al, 43). This pattern is similar lo volcanics now
being erupted around the Pacific margin in association with convergent plate
margins.
2. A major change to fundamentally basaltic volcanism (including bimodal
mafic-silicic associations) look place during late Cenozoic lime al aboui Ihe
inception of Basin-Range faulting (Christiansen & Lipman, 12). The transition to
Ihis new volcanism began in Ihe soulheaslern part of Ihe region and moved norlhwestward. The lime of iransiiion may be correlated wilh Ihe initial intersection of
the East Pacific Rise with the continental-margin trench syslem, an inierseciion
which Atwater (5) also interprets as having progressed northwestward.
3. The composition of the crust and upper mantle as il existed beneath ihe
Colorado Plaleau prior lo Basin-Range faulting has been ingeniously reconstrucled from crystalline rock fragments in a breccia-filled diatreme, which is about
30 m.y. old (McGelchin & Silver, 45). The crusi contained about 31% intermediate and acidic igneous rocks, 66% basic metaigneous rocks, and 3% eclogiie.
The upper mantle lo a depth ofabout 100 km contained about 75% peridoiite
and pyroxenite and 25% eclogiie. It is especially interesting thai the mantle 30 m.y.
ago contained this much eclogite, because eclogiie is capable of converting into
gabbro wilh a volume expansion ofabout 10% in response to a rise in temperature
or decrease in pressure.
Eclogite may be a key to an undersianding of laie Cenozoic uplift of Ihe broad
region ihal includes Ihe Sierra Nevada, Basin and Range province, and Colorado
Plaleau. The expansion of eclogiie in only 60 km of manlle could produce an
j
'
'
;
'.
'
'
I
,
234
THOMPSON & BURKE
uplift of 1.5 km (60 x 25% x 10%). The former eclogite may now be represented by
gabbro dispersed in the manlle low velocity zone, or by crusial additions of basic
metaigneous rock, or by basallic volcanics.
SYNTHESIS AND TECTONIC MODEL
TTie regional geophysical dala pul many useful constraints on speculations about
the fundamenlal lecionic processes of Ihe Basin and Range province. Among
ihese dala ihe heal flow is central; the volcanism, Ihin crusi, low manlle velocity,
accentuated low velocity zone, generally high elevaiion, subdued magnelic
anomalies, high eleclrical conductivily, and greal breadth oflhe seismically active
zone can logically be associated wilh high lemperalures and high heal flow.
The graviiy data—coupled wilh the estimated extension—supply an interesiing
consiraint that does not seem to have been widely recognized (Thompson, 77). If a
30 km crusial plate were simply atienuaied by a horizonlal extension of 10%, a
negative isostatic anomaly of more than 3(X) mgal would be produced. If Ihe
allenualed plale were only 10 km Ihick the anomaly would still be 1(X) mgal.
Because Ihe regional isostatic anomalies average no more than about 10 mgal, the
graviiy emphalically indicaies ihal Ihe circuits of mass flow must be closed. Nearsurface crustal spreading is almost perfectly matched by lateral backflow in the
manlle.
If we imagine a verlical fence surrounding Ihe Basin and Range province and
extending through the crusi and mantle, the integrated flux of mass through the
fence musi be zero, despile Ihe oulward flow by exiension in Ihe upper crust. We
now need to find oul how the deep lateral inflow takes place. Is Ihe lateral flow
in Ihe low velocity zone? Is il a deeper manlle flow associaled wilh narrow
upwelling convective plumes, analogous lo a ihunderhead in Ihe aimosphere? Is
Ihe flow relaled to former subduction of an oceanic liihospheric plale al Ihe
conlinenlal margin? Al present these questions lead rather quickly into sfieculation.
The regional geophysical characleristics, geologic history, and petrology rather
strongly suggesi a link with plale-iectonic interactions al Ihe western edge of ihe
coniineni going back lo early Cenozoic time. Analogies wilh spreading marginal
basins of Ihe western Pacific are especially promising (Karig, 40; Matsuda &
Uyeda, 47; Scholz el al, 64; Sleep & Toksoz, 68; Thompson, 77; Uyeda &
Miyashiro, 80).
The general idea is Ihal in a broad bell on the continental side of an arc-trench
syslem, a descending liihospheric plale either generates magma along iis upper
surface or creates a convecling subcell by viscous drag. TTie rising magma' or
convection current helps lo move the arc away from the continent, creating a
spreading marginal basin. The silualion is somewhat differeni along the central coasl
of North America in that subduction ceased when a spreading ridge reached the
trench in middle Cenozoic lime. Bui because Ihe descending young lilhosphere
would still be very hot when Ihe ridge reached Ihe trench, and because conductive
heat transfer is very slow, il is easy lo imagine Ihal Ihe ihermal effects of a pasl
subduction process are slill being fell in Ihe Basin and Range province.
riEGIONAL GEOPHYSICS OF THE BASIN AND RANGE PROVINCE
235
ACKNOWLEDGMENTS
We thank David Warren for allowing us to use his unpublished m a p of crusial
I h i c k n e s s ' ; John Lahr and Peter Slevenson for Iheir m a p of earlhquake epicenlers;
and Kimberly Bailey, James Baxter, Roberl Daniel, Allan Lindh, Dohn K. Riley,
Don C. Riley, and Donald Steeples for stimulating discussions in a seminar which
ranged widely over many o f t h e topics discussed here.
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65. Sclaler. J, O,. Franchcleau. T. 1970, The
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mediate distance ranges. LfS Ceol. Sum,
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C A:- 1 . V )3l% • ^ : ^ i ^ n ;;.;4 3 :,-;':0..^-35;. 6;S;8 ^il2:0-:65 4:.,P AS 0 -"OE -IR-OBLES''- HU D ; B ' A J H ; .S PR I N GS'-^';. ; • - - . ^ b f i .
• . t k f i - 2 . , r g r , S ;-^.f.9:2. '^;^3:3 S^^X .,3'5-^-5.82'i•i:2-0-;666:'S ANTA-' 'YSAB'EL.: SPRIMSS-..f;SUi:PHUR-: ^PR-)."'.;\.;?-|f
c A .Jt.>:.'-93' i S ^ s s •%3.4^v:;^j^o';;3:5'?2,6;9%X2-0:i,8:5X->:PEi;,H'Os''W,^^^^^
-"^i^-^t: • v;'"-:'^w;—v-'^l'^t^S
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ttdi.)
SPRTN^&S-''
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Ok -.iirS ;• ;; •-; ':'l:3i5 "^•'^7 • • " • ' i : ' : ^ ^ ^ m . . M ! 2 B . ^ i X i ^ M i ^ f ^ -V*L,LEY ^^=0:7 SF-R:Is!«G;S •'': •'..^ -•-,.. :. •' C- .^^rs •••'-CA:,:..6 - ' i m - i r y ^ k , ? ^ •'•i^T'^l 1 '^'35.;'122'!l^0V:5'4'^^ "NE.S/SiO'M'^-S'-:tARR.OYO'^'S.R^ft.N'DE) S;P;R;iN^S" " '%• fes^'iS
C A . - - I .,X4;0A-. . i i ^ 9 3 •-,,^33,i'>i-/;3:i&.-:i6tS:^M;i:6^9a3\ KEENEf.U'ON:DCR;:;S'P'R;i.NG.S" •';;..
'^•••^^:^::::i^t'-:'^^'^<^'^r'^
CA.-^M,, . ^';.-^ Q,^
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••,PA-.^^''2.; •'^'>,v,;...:X:2b ,; 48^-?;fei - ; 3 . & . , s i 4 j f ; i i 7 . . 7 6 3 :?'kLn-"^w^TnG^'%'^:K'----At'''r'&k'^--^-^^^
;CA.., 3.-.13>9. A'^IXO . ^43::l!;i;.,#^^id:&->lX7-.'7^1.:;L6,WE'R-v,tB.U^
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CA.r:.4::--i:-!^vv^j.. L^M:X3&,sm^::ir7Ȥt^9':QjRxr^iSQtK^'^^^
-.spRiNff .'.••:•••••.•>-;:*•-i'w:..;;' '^'••
,CA -.-S 1 4 4 : ; . .„v,^^0. 26-,.-;i 3.6:, 12:2 :;li:7.:21i7..WARH.,'S-ULPHUR\S-PRIN&S,-^'-^:i-: " " ^'V-'V^:-'; • ';'-|-i-;->:'v^';
•CA'''--6 ,14.2->-;>.•„' . •• ,V,„";VBVX^;3:6--0-45- 1 1 V 7 - . 7 6 ; 9 ' . C 0 S : 0 " ' ' W 0 T ' . : S P R I N G S . . , . ,-" ' • " ' " - ,'. '•-'•.:::'>.. -jvi,.-jS^i^'^ •"'-.•^
CA • 7 r 4 X A ::;2 06
96 1 • 3 6 ^ 0 35 1 1 , 7 . 8 0 2 OEVTLS KITCHEN • .- ' . j ' " ' ' '
' '^t^ ?-^r • "' J " :" ''
.CA -•8.:a-41.,;.;:-"-2.0 3 •;94.;;.--l 3-6* 0:31 •••ri7,..833- rFU;MAR-aLri ""-T ''^' ' : ' ' - r - - ' .''' ^''t'^r^ '• • ' > ' * " ^ ^ - : '
CA .^l-';X35.;.v,,12;3
• 5 # . , . - 1 . 3 6 ' . / ^ 7 ; T - X 1 8 . ' 4 - 0 : 4 . ; K ' E , R N : ? ( ; J O R D A N ^ ^ •H:dt"'-SPRIN'G--, '.• "c'-^^'^'.''.'-^'-."•:-;:^
CA :;;2 ; 1'3'6: .;:',I0O -..37 .-rM'^ 5 6 . 2 1 0 : i l 8 . i : 7 6 ..SdDA,.'SPR rN:G;s ' (MON ACHE. vMEAD-OWS ) ' • "
'.;---.--'';'
C A , , : 3 , ; i 3 4 . ; •;77 .-V24---/1 3 6 . X ¥ 9 X1.8..6,56 'HOOREHOUSlE SPRINGS , .: Z-.. • '.'
•••*;'-'. ^
z";^--/
CA : x ' c - . • • • ; ; - - ; 8 i
^ T . - ^ a :3:&.765- . i 2 p * - 9 o i . . ; ' . ; , • ; . . •
••..••.:.,.'., - •''>• • ^ ^ • ' . • - " • • - . " ^-'^^'• •' •"••-^^
• CA , 2- 1.3.2.. V l l ' 9 , 4 ^ 8 ; M ; . - : y 6 - 7 0 5 : i2O.."860 MERCE.Y .HOT . SPRINGS . - V • ; • '"^:'-"-"•'••.,'•';''•/•;c.A " 3-';';-'-\^^,. :-7'5 _,:.23" - .p-5-6.^,6.4vP';;i2:o-.v6SA • :' .J''-"^^;-;-^^ ;v •-..-•.•••>"'••'•'^- • . " ^ ^ i : - : • < ' • • ' : , • .,
CA-;'4v 1 3 3 : - ; X 1 2
¥ 4 . : • 1 3 6 . 1 4 4 ; 1 2 d , . 5 5 5 ; COALINGA MINERAL (FRESNOt HOT) SPRINGS
'-.
CA . 1 -.•:^;. ; .,,*^77 •;24' -1 3 6 . 9 3 8 ; a . 2 X ^ 5 6 5 -SARGENT E S T A T E ; ; ' ';:-:;':, . v .: . .^ ^v^'-,:. „ • / ' ' " - • ^r
CA
2 , - ; / . 1 0 0 . 5 T : : 0.36-1^:19 1 2 1 . 8 4 6 s t i L P H u ^
. \ ; • ?. .; '"^ '
•
; \
':'^^g^:,:^'.M,
TEMPERATURE
' ' S o -
«
=
"*
t!<
CO
a «
o:
NAME OF SPRING.
-r
'CA
3...--9(I-k 114 ;:;;45* 0 ; i 3 6 - 3 3 3 ; r 2 1 . 3 4 0
' ^^ • ^•^''^••
CA
4
9.2 .: . 9 8 C 3 6
1 1 - 3 6 . 3 3 3 1 . 2 1 . 3 6 7 PARAISO HOT" S P R I N G S
;: V-.
VCA
5
91
1 4 4 . ; ; : 6 2 . - 1 ; 3 ^ . 2 3 4 1 2 1 . 5 4 6 T A ^ S S A J A R A : HOT ;SF»RINGS :
'
'.'•':;:'>:r
CA ^ 6 ' " ? 3 , . . . 1 2 2 j 4 9 a . r ; - ; 3 6 . 1 2 2 i 2 1 . 6 3 8 , SLATES r a i G ISUR) HOT S P R I N G S ;
':• i . .>
, : CA - , 7 ^ 9 : 4 . . . : . . 9 U : ; 3 6 . . : a i i 3 6 . 0 8 4 : 1 2 1 . 5 8 4 O O L A N S ^ K O r S P R I N G . ,. ,
.--. ^^ i.- ;'r-x,
;\CA . 1 1 4 0
100 •:'37 • l , ' : 3 7 i 0 2 9 ; i l 7 . 5 8 3 . . G R A P E V I N E SPRINGS
.
.if." " - j ::^|if^"
/ G A l
' . . '
>.;. . H r ; 3 7 v 9 7 7 - 1 1 8 . 9 2 6 ; ( H 0 T . " S P R I N G ) - - ^
...'•.•
••''W^.''\'^^"h'-^.
• CA . 2 - : 1 2 7 A ; 7 0
2 1 _ : 0 : V 3 ' 7 . 8 8 4 ; i l 8 . i 4 & 7 . : B E R T R AND BRANCH ' " r ' ^"z
,
V ":
- ••
•CA
3 127..
134
57
.1 3 7 . 8 0 2 1 1 8 . 5 3 2 BENTON.HOT S P R I N G S ; - .
; ;>: .
CA
4 .
, :-L.75 ; 2 4 , : . l ; ^ 3 7 . 7 1 9 i l l 8 ^ 7 3 5 ( S P R I N G S )
;\:... , . • ? .
'^^
" ^ ' c
• CA
5-;
,67 .20 : : v l : v 3 7 i 7 0 B . l t B : . 8 1 3 . C H O T , : S P R I N G ) " " : ' ' ' : •
. , , , [}
;.:.
,' CA -6 1 2 2
179
8 2 - X l 3 7 . 6 9 2 1 1 8 . 8 3 9 L I T T L E " HOT C R E E K ' S P R I N G
• :';.
; CA 7 V . . ; 1 2 3 v . 5 2 . ; 0 . . 3 7 . : 6 7 7 . a i 8 . 7 9 O . . D E H Y : „ H O T . S P R I N G ANO QTKERS V. \
- ' v
1 ^ - ' ' ' C A ' * - 8 ; ' • - . ; • / • " 1 2 7 . : - 5 3 ; : . 0 > 3 7 b 6 6 7 1 1 8 . : 7 8 l ; - . ^ E ' " " " ' " ' " ^ ' " ^ ' " ~ " ' ' : . . ^ ; ..-.-;..- • , . , - - y ' . : ' : ' ' : ' v - j : H .
, Zh
9
'\.
, 1 9 9 .93
1 ; 3 7 . 6 6 5 1 1 8 . 8 2 8 . HOT CREEK S P R I N G S
.
-,....
.v?
CA 1 0
^^
166
7 5 ' . 0 3 7 . 6 6 4 1 1 . S . S 0 2 . T H E ' TU3 AND OTHERS
. *
. >
' CA 1 1 ;
'i20,;49
0 ;37-657.118.764:..
i.;:v.- . ;
; • ;'
, ' '. •
.... z^:
:' :;.
. : CA 1 2
1 7 0 ^ 7 7 ' 0 3 7 . 6 5 6 1 1 8 . 8 3 4 HOT CREEK S P R I N G S . - •
-^^v- • ^ ; .
CA 1 3 .'
• 71
22 . 0 37v653 .118^925
V l.r;:'
-.
;'
; CA,,14;i25
129
54
1 . 3 7 . 6 4 8 1 1 8 . 8 0 6 (HOT'SPRINGS)"" ;'
"
" . : • - • . . ;
CA 1 5 1 2 3
199
93
I 3 7 . 6 4 3 1 1 8 . 9 1 4 C A S A / D I A B L O HOT S P R I N G S AND G E Y S E R .
CA 1 6 . 1 2 4
. 1 5 4 : 6 8 ' 1. 3 7 . 6 4 7 - . , l X 8 . 8 5 9 CASA. DI ABLO HOT P O O L
.,4.:
:CA 1 7 ,
.,
; 85
30 : 0 ' 3 7 * 6 3 9 1 X 8 . 7 5 5
, . - - . , . .
.
, ^-^.
,
CA 1 8
-73
2 3 , 0 / 3 7 . 5 3 8 ' 1 1 8 . 8 8 7 CHANCE SPRlNff
. ; • , / •
''
, ' ;
;'•••CA,.i9
. • : ' • • ..'.62. 17 ;o , 3 7 . 5 3 8 ; M I 8 . 8 6 6 .
•,••..;.„'-;.••:•.•,...•..-•;,''-'\c--..^:^..-Z'-':}Z,:'
. CA -20
1 2 7 ' ; 5 3 : a . , , 3 7 . 6 5 5 • . 1 1 3 . ^ 7 2 , 0 , .>-V;-~-^'^"-^:'^-.-;-T'-'V^"V.^ •"•'-/
' • • - ' • ' ; • ' : ' / ' '->•"•'
CA 2 1 , 1 2 6
94-: 35
I . 3 7 . 6 3 0 U l B . 8 0 8 WHITMORE H O T - S P R I N G S ..
• ' /
'^^
• CA 2 2 '
.
• 73
23- 0 ,37.607 ar8..808
..*^ > : . - • . ; . -^'.-C
•- \. — " . • • , -"^^
CA;23
62
17
Q,37.557 118.705 . .
"•;
-- - v - - •.. " ' " } . ' • •
CA 2 4 1 3 8 . 1 3 0
5 8 . 1 : 3 7 . 2 5 3 . 1 1 8 . 3 7 3 KEOUGH HOT; S P R I N G S
.:..%;;;?..
•CA 25 ,131
;109.;43
1 . 3 7 ^ 2 3 4 . 1 1 8 . 8 8 1 BLANfEY; MEADOWS HOT S P R I N G S . ' ' • .
. "\".
•CA , 1
H O 3 7 . 9 9 7 1 1 9 . 0 4 5 PAOHA ISLAND FUMAROLE.
..
~•CA
2.120
20 2
9 5 ...0 , 3 7 . 9 . 9 7 1 1 9 . 0 2 0 PAOHA I S L A N D S P R I N G S ,.
^ - . ,
\ V '
CA. 3 . . . . .
H 0 . 3 7 . 6 2 2 , 1 1 9 . 0 2 : 8 FUMAROLES ' , . . . " •'•
.
'•
•CA-. 4 128
.,X20
48
1 3 7 . 6 1 8 1 1 9 . 0 7 4 REDS MEADOW -HOT S P R I N G S
CA. 5 1 2 9
.110
.43
1 3 7 . 5 3 2 1 1 9 . 0 2 5 F I S H C R E E K HOT S P R I N G S
'
:.
CA . 6
. 9 5
34
0 37-414 119.140
.
, ; :
CJ-
•CA 7 130
111
CA 1 .86 . 96
CA -2 87
80
GA • 3 88.
84
CA 4 39 ;i06
CA 1 .85
81
CA 2 84
90
CA 1 121
91
•CA 1.113
145
•CA '2 114
143
•CA .? 116
157
i^
44 I '37.327 119.018 MONO HOT SPRINGS
35 1 37.847,121.635 BYRON HOT SPRINGS
26 ,0 37.503 121.904 ALAMEOA WARM - (MISSION SAN JOSE HOT) SPRSi.
28 1 37.398 121.794 MINERAL "(ALUM ROCK PARK) SPRINGS
41 I 37.103 121.478 GILROY HOT SPRINGS . •
27 0 37.924 122.046 SULPHUR SPRINGS
32 .0 37.880 122.627 ROCKY POINT SPRINGS '\
32 I 38.033 118.902 MONO BASIN WARM SPRINGS
63 1 38.699 119.845 GROVERS HOT SPRINGS
62 1 38.343 119.400 FALES HOT SPRINGS
70 1 38.244 119.205 TRAVERTINE HOT SPRINGS
•*;•/' s-:Vii^-^
--^•-^-JT^•^
'^'^':. • : - . - ' ^ . ' ^ : ^ ^ ' ^ ^ : ' M y , : ' ' '?-!v\.-.'?:-^.^'''s-.^:-^tt^'.'.:
' ... V-
TEMPERATURE 5 !
t*.
V>
NAME OF SPRING
CO
(.'•
4 11'5
• CA
147 '64 : 3 8 . 2 3 7 1 1 9 . 3 2 5 BUCKEYE HOT SPRING .
CA
5 117
3 8 . 2 2 3 1 1 9 . 2 1 7 THE HOT SPRINGS
;ii3 4 4
C A • S ' ' l l i 8 • 10 0 37
3 8 . 2 X 0 1 1 9 . 1 5 1 WARM SPRINGS FLAT CA
7 1L9
3 8 . 2 0 3 1 1 9 . 1 1 8 (VtARM ;SPRING) •
100. :37
•CA
8
,
,
6
3
"
3 8 . 0 4 6 •119.080 :BLACK POINT HOT SPRING
1451
1
3
A
23
,
1
3
8 . 1 9 2 .120..827. VALLEY SPRINGS
„ CA
.,.,.
75
_.tW
„• - 7 . . : ^
1
3.8.99.4 ' 1 2 2 . 7 4 5 - ;;„ -..-. • ; . . . : ; , - . ••, CA
.
1
2
2
.
7
3
4
'
•
:
'
]
"
•
•
•
•
'
^
'
•-•••
•,•-•
;-'{.:;•
O i 3.8 .-98 2
•
W
• C A \2
3
- CA
;.H 0 3 8 . 9 7 9 1 2 2 . 6 5 9 (FUMAROLE)
.38.963 122.724:
. CA 4
'"
• i ' ^ : W; . 3 8 . 9 . 5 6 1 2 2 . 6 9 9 C A •. 5 '
,-.::--W v 3 3 . 9 5 0 1 2 2 . 6 5 4
CA ;: 6 •
. 82 -•27-:/ v ! 3 a . 9 3 6 1 2 2 - 9 0 7 HIGHLAND SPRINGS .:;! '
. C A :--7. 52
8. ,54
3 . 8 i 9 l 6 1 2 2 . 7 9 . 9 CARLSBAD SPRING ; . • - : •
.^ ,'
CA
...76..: 1 2 4:/
3 8 . 8 9 2 X 2 . 2 . 5 3 3 BAKER" SODA SPRING
• CA 9.
1.73 ;:2;4.:'
:^'' /. ;- . . ,V "
59
• CA 10
123. u52.., i 3 8., 3 7 3 . 1 2 2 . 6 8 9 SEIGLER SPRINGS ,
11
,5
8
.113 .44 ..^^ 3 8 . 8 5 8 . 1 2 2 . 6 7 1 HOWARD SPRINGS ;
. CA
,12
3 8 . 8 3 3 12 2 . 3 5 7 ONE SHOT MINING CO.
.71, ,22 '".''V'"•CA
13
,38
.re 02 . 1 2 2 . 8 1 0 THE GEYSERS
72
.
:B
.
/ •:
CA
73
12 0
48.
38.788 .122-777 SULPHUR CREEK
- -'- CA 14
48 .
12 0
33.785 122.655 HARBIN SPRINGS
. CA 15. 54
128. 53
38.773 122.705 ANDERSON SPRINGS
CA 16. 63
160
74
71
38.772 122.755 LITTLE GEYSERS
CA 17
163
62
72
33.768 122.717 CASTLE ROCK SPRINGS
CA 18
80
33
38.655 122.484 AETNA SPRINGS ,.
• CA 19
.91
' ' ' ',;"
38;652 122.355 WALTER' (WALTERS MINERAL) SPRINGS
19
• C A 20
66
- 3 8 ^ 5 8 0 122.575 CALISTOGA HOT SPRINGS
• C A 2 1 ' 81
,17 2
77
75
• CA 22
8 7 31
3 8 . 5 5 0 122.720 MARK W.E5T SPRINGS
83
• CA 23
7 8 26 .
3 8..519 122.256 NAPA ROCK (PRIESTS) AND PHILLIPS SODA SPR
82
• CA 24
90
32 .
3 8 . 4 9 0 ,122.498 ST. HELENA WHITE SULPHUR SPRING'"
-V \
• CA .25 76
87
31
3 8 . 3 9 2 122.552 LOS GUILICOS (MORTONS) WARM SPRINGS
• CA. 26
60 .16
38^391 1 2 2 . 2 7 9 (JACKSONS) NAPA SOOA SPRINGS
C A 27
77
3 8 ; 3 9 1 1 2 2 . 5 7 0 MCEUEN R A N C H W A R M SPRINGS' " " • " " '-'"
73' 22
CA 28
78
70
.38.350 .122.515 SONOMA (ELDRTDGE) STAtE HOME WARM SPRINGS
21
CA 29
76
3 8 . 3 3 9 1 2 2 . 2 5 9 (NAPA) VICHY SPRINGS..
24
CA 30
33- 28
38.324 1 2 2 . 2 5 8
CA 31
79
115
3
8 * 3 2 0 1 2 2 . 4 8 3 AGUA C A L I E N T E AND F E T T E R S HOT S P R I N G S
46 ,
CA 32
79
112
38.311
1 2 2 . 4 7 1 BOYES ( O H M S ) H O T S P R I N G S
44.
• CA
60
3
8
.
9
1
0
.123.307
1
(OLD) ORNBAUN SPRINGS
16
47
• CA
3 8.'87 4 1 2 3 . 5 1 8 P.OINT ARENA HOT S P R I N G S .
111
2
44
CA
70 ,
100
3
3-8.300 1 2 3 . 1 7 0 HOODS ( F A I R M O N T ) HOT S P R I N G S
37
• CA
71
13 4 57
4
3 8 . 6 9 1 123.024 SKA5GS HOT SPRINGS
CA
108 4 2
1
3 9 . 9 2 7 1 2 0 . 5 7 8 D O Y L E HOT S P R I N G S
CA
163
41A
2
72
3 9 . 7 5 5 1 2 0 . 3 5 9 M A R B L E HOT S P R I N G S
CA
3
42
86 29
3 9 . 7 2 8 1 2 0 . 5 4 7 MCLEAN SULPHUR (WARM) S P R I N G
CA
111
4
43
43
3 9 . 5 7 2 1 2 0 . 3 4 8 C A M P B E L L HOT S P R I N G S
CA • 5
H
3 9 . 4 2 5 1 2 0 . 0 2 5 (STEAM V A P O R )
• C A -6 44
139 60
3 9 . 2 2 6 1 2 0 . 0 1 0 B R O C K W A Y t C A R N E L I A N ) HOT S P R I N G S
" < . • ' . ' " • / •
.w
c
- • V- .ill
'rrrT-f riP^ii^^-xi:-s.\\s..
V
TEMPERATURE =f
r«e
U
UJ
2
^
•^
NAME OF SPRING
CO
44 A
75
' "^CA 7
76
1
. "CA
62
;; - C A
2
4:8 A
/••CA
78
3
• C A : - 4 . ,48..
10 5
, * C A .-.5
. .62
6
4;9
. •92.
:;. • c A
r " C A ^^
60
51
.74
8
-. CA
65
9
78
^ "CA
51A
, r , CA 10
70
^ / -CA 11
-•. CA 1 2
69
153
" • • C A 13 , 58
X39
6 6 .. 1 2 0
• .CA.
/85
• : CA 15
:J:>CA 16
; 80.
r ^ C A :i7 .55.
:„.87
57
X55
• C A IB
.70
'•• C A
1 4 5A
CA
80
2
,103
•CA
3 ,45
89
- •CA
4- 4 6
70
• CA
1 29 A
; .CA
2.
72
. CA "3
204
30
,• • C A
2 0,5
4
31
•CA
204
5
CA •• ^6 ' 32
100
39
CA
1
22
7;
2
5
15 0
; CA
2 27
199
' CA
199
3 26
CA
148
CA
.4 36
CA
205
5 34
, CA 6 . 35
83
190.,
. :CA
7 37
38
205
. CA
8
203
CA .9::
33
202
• C A 10
40 .
100
CA 11
67
• •CA -1.
8
5
4
5
8
•CA
2
101
CA . 3
CA
1
109
. CA
2 12
114
CA
3
CA
73
4
4.
ao
- '
.
•
.
;
*
•2 3.-:
25 .
3 9 . 0 1 5 " 120.338 WENTWORTH SPRINGS ;""^''*'
3 9 . 4 3 0 . 122.538 SALT SPRING-ANO SULPHUR
17 ;
J39.413
26
,39.343
41,
,39.292
17
.39.255
33 V
,39.196
16
39.174
23
39.171
3 9 . 0 85
25
39.075
21
21
0739.064
67
1139.057
60
1 39.037
:4.8
-39.03.2
30 •
39.022
•26
39.019
30
39.008
69
3 9 . 0 02
39.699
21
39.663
26
39.227
40 ..
39.165
32
4 0.580
21
.40.568
22
40.364
95
40.355
.96
4 0 . 3 02
95
4 0.245
37
4
0.i42
49
4
0
.457:
65
4
0
.455
93
4 0.4 4 7
93
4 0.444
64
40.440'
96
40.44 0
28
40.434
87
40.421
96
40.393.
94
40.382
95
4 0.019
38
4 0 . 6 73,
20
40.238
30
40.223
38
W 1 '41.959
43
46
25
0 .41.873
1 41.360
1 41.828
""•122.977 SODA 'SPRING' :'""\
122.668 FOUTS SRINGS ' (RED EYE AND CHAMPAGNE.SPRS.:
122.821, CRA3TREE HOT ;SPRINGS:
- ;
122.526 COOKS SPRINGS' , , .
122.714 NEWMAN .SPRINGS
122.98 0 SARATOlGA SPRINGS
122.511 COMPLEXION SPRING
'.
122.459 DEADSHOT SPRING
'-7-122.580 CHALK ,M,0UNTAIN - '
122.595
122.475 E L G I N ; M I N E "
" " "."'"
122.4 2 0 WILBUR.SPRINGS^AND OTHERS
122.432 BLANK SPRING .
,.;.,.
122.44 4 ABBOT MINE
122.581
I. ,• 122.789 BIG SODA (SODA BAY) SPRING . •
122.654 SULPHUR BANK
;...;[ • •'
123.482 ( S P R I N G )
••
' -"*•;••'•
' 123.584 JACKSON VALLEY MUD SPRINGS .
123.362 ORRS.HOT SPRINGS-.' . \ .
: ^ ,123.159 VICHY SPRINGS
120^265 TIPTON' SPRINGS
-...',
120.325 SELLICKS SPRINGS
,
.".
120.243 (HOT "SPRING)'•
.••
.- - - „
120.257 WENDEL- HOT SPRINGS
.:
--,.•-; '•. — [•'120.195 AMEDEE HOT SPRINGS ' • ' . '
12 0.006 HIGH ROCK RANCH SPRING
*
...
120.935 INOIAN VALLEY (KRUGER)'HOT SPRINGS
121.545 H I L L C R E E K SPRINGS ' V
'; ,,
•
121.501 BUMPA'SS.HELL (BUHPASS.HOT SPRINGS) •
121.53 6 SULPHUR'WORKS~(SUPAN S CTOPHET HOT) SPRS.)
121.40 9 DRAKESBAO~(DRAKE HOT SPRINGS)
121.434 DEVILS KITCHEN '
121.420 HOT SPRINGS' VALLEY •
121.399 BOILING SPRINGS LAKE
121.375 TERMINAL G E Y S E R "
121.507 GROWLER HOT SPRING
121.513 MORGAN HOT SPRING '
"
,
121.0 36 (SPRING)
122.634 .SALT SPRING
' /
122.110 TUSCAN (LICK) SPRINGS
122.747 STINKING SPRINGS . , .
120.936 (WARM SPRING)
120.163 PETERSON RANCH
120.158 FORT BIDWELL HOT SPRINGS
120.917 POTHOLE SPRING
L .
/Sto
ca
TEMPERATURE ^ !
I*
S»2
S
2
I^SS^S
2
«
-1=
»3
=»
^
-3
H^AME 5 SPRIHG .
r CA :; 5..-,13' '
67 .^20
1 .'41^726 1 2 0 . 0 8 1
!«CA
6
1 4 . . "206
97
1 41-&70.X20.205
CA
7 :., 16 -; ,.18.3
87
1 : 4 1 i S X 5 : : X20,.X02
CA . 8
1 7 :; : V l 5 0 1-^66
141.1500 120.083
; CA
9 ; 1.8 .;•.!; .208
98 : L . 4 1 . . 5 3 4 : i 2 0 . 0 7 8
CAIO'
6::^.f^.'.;gi.,. 3 3 ; - l 4 - r - 4 9 2 ' . 1 2 0 - 7 0 0
BOYD HOT SPRING '
LAKE' C I T Y ; (SURPRISE VALLEY) HOT S P R I N G S ; '
.SfcYFERTH HOt" S^PRINGS
. ; .^- X::..'^:. • --J-li
LEONARDS H O T V S P R I N G S
:/:
r;''-.;
HOT .SPRINGS .'(SURPR I S E VALLEY ; A N D B E N H A C ) -.
HOT CREEK
ESSEX S P R I N G S , , . . . . "
-.'.CA •ii--;'--7;/..v-':.;.8i.:^r27=.^'i/;4;i.-484 x2o.76"4- (SPRING).
•.•.;.-.,. :•,?'•.: .".-. ::ri-,y-<. \'-''^-"•;.;;;
CA.'X? ' 1 0 , v - , . ^ ^ ; 2 2 . , l - 4 I - 4 5 ' 2 ^ X 2 0 . . 5 X 5 (SPRING) . - - c - ;
\ Z : : ' . .•.••:•/'f
'
• CA i 3 : - : ; i ^ 8 v . ; 2 C 4
9;6 1 4 1 . V 5 0 „ 1 2 0 . & 3 4 K E L L Y HOT S P R I N G
• ; - ; ' " . . ''''•
CA 1 4 . 2 0 . •'.138 r 59 v;i 4 1 . 2 6 6 1 2 0 . 0 8 0 MENLO. HOT SPRINGS
".
,^.:.
.
;;/
CA .15. V - ' : ; ; < ^ 7 5 - . . 2 3 V l 4 I ' » 2 5 2 . . X 2 0 . 5 2 1 .(WARM SPRING);
;,
'•/; •
/ - " v / ; * , / : : ' :/;/^
CA 16 ; / 2 1 / / 1 0 9 - :43 :;70/4r^219-120.06BSQUAW7^BATHS : V ' v ' ' V , ' ^ . ' / ' '
• •;-;l^i:^
. c-A .17 •^'....:„.;1-'..., - :7> -w'^';:iv'4i;it95:i20.475.^(spRiNGs-)..-'";--':?-'':'%-Vv.' :*r-•
••••^•'-•'•.r-:. ^" ; 7 -74^
CA ;18 .n
^^ ;;17O^:i77/5 0/5:l»190A;i20;383 W E S T ; V A L L E Y R E S E R V O I R H O T S P R I N G
^
•^'
CA 19 ; 2'2/^;: -70 :".21.. =:0;Vl.-167,; 120.0.32 B A R E - R A N C H .
{v i. .;_ .\ ?. ,n, .;....^.^7.- -;;:;;v:^. . ::^
C A ; 20 .:,.,.,;;:;•-.yo .'^Livil^^iilisO- 1 2 0 . 4 0 3 (WARM S P R I N G ) '••:•..--.-;'/v
'V;/-:/^:
CA -v.. 1 : .• ^ 3A.-.::i9i.;,: •88-rai.J.'4.i.60 7-. X.21,.523 'HOTrvsPOT; -';'-r' "^^-^-h-:- ' -'Js^^'V
CA
. CA
. CA
• CA
•CA
CA
CA
CA
; 2: -ll.,:-:Sl70 /77 ' 1*,41.229 121-405
3 2.8 . -174 79 "1 41.143 121.110
4 ,29 . ..174 , 7;9 T. ,41. 1 26 .121. 028
5 .23 ." .136 ; 58 ,1 41.036 121-924
,6 ,24
179 8 2 . 1 41.025 121.924
\7 . ,•';.;:. .r H I 41.012 121-274
. 1 - 2 ,152 66 1 41.973 122.202
2 , .2A',.76 24 1 41.919 122.369
/;•.-/;'?:'-v •v-'^-:;^ :;'^.^.:
LITTLE HOT SPRING " > ' "^ -: " /4p v .:^' ^ .'•
BASSETT HOT SPRINGS -•
"/
KELLOG , ( S T O N E B R E A K E R ) HOT SPR INGS^
HUNT '(KOSK CREEK) HOT SPRING ...BIG BEND HOT .SPRINGS .....
....-'•>
(HOT : SPRINGS)
. '" ;'"-'1
KLAMATH HOT SPRINGS
.
'
' /'4
BOGUS SODA SPRINGS
'•.'.i'r' ."••'.•..."• - ' j y t ^ '
CA - 3 .
3
, 184. ,84.: 1 ,41.407 1 2 2 . 1 9 7 (HOT :SPR ING ON, M O U N T S H A S T A ) ;••' '
CA ,,.i:„ .1 ./:.;,., 8 4.V,,-28 : X . 4-li659 ,123.319/SULPHUR .SPRINGS...-;,,!, '..j., :••. . .j^S'?^/,-
..
- --.
. • „ , -•• .::...-• - C O L O R A D O
-..-•
. ; - - " • . : ^ < ; i ' . ' U ' : : ' ' ' ' " - ^ ' //..-^ /.'^••.: • : ^ • • • ' V , / • , . , ^ • ' ^ ; • ^ / . . / ^ • ^ ^ ^ • • / ' : : ^
CO 1- 44 /•- 67 • 20 : 1 3.7i294 105.784 DEXTER-WARM 'SPRING
. ' ,:^ -. 7 , <
CO 1 . 33
85 30; 1 37.751 10&.317 SHAWS WARM' SPRING
v^'r
-'>A f^ . ; % ; -;
•CO 2 31 >X34 57 ; 0.37i754 106.828 WAGON'WHEEL GAP. HOT SPRINGS , > CO 3 V 32 , •X03 • 4.0 :\X 37.511 105.945 RAINBOW HOT SPRINGS ...^
, *- :-; ^^.^
CO 4'- .41 ,...80 27 . 1 37.033. 106.805 STINKING VSPRINGS
-.'
^"
CO .1
.",89 32:.l 37.741 107.034 ANTELOPE WARM SPRING .
. -V •
CO 2
85 30 0,37.718 107.060 BIROSIE WARMSPRIN5 (2) CO 3.- 34
- 91 33- 0 37.453 107.803 PINKERTON HOT SPRINGS
CO 4., 35 ; 111 44 0 37.400;i07.849 TRIPP HOT SPRINGS
CO 5 35
.96 ,36 0.37.391 107.846 TRIMBLE HOT SPRING
•.••.•'
• CO 6, 39
135 58 1 37.263 107.011 PAGOSA SPRINGS
.
'
"'
CO 1 29 -111 44 1 37.771 108.091 DUNTON HOT SPRING
CO 2
. 82 28 0 37.762,108.113 GEYSER WARM SPRING
.
•
GO 3;
114 46 0 37.752 108.131 PARADISE HOT SPRING
CO 4 30
111 44 0.37.689 108.031 RICO HOT SPRINGS
CO I
22
91 33 0.38.487 105.912 WELLSVILLE WARM SPRING
CO 2
82 28 0 38.479 105.891 SWISSVALE WARM.SPRINGS (2)
.- ' •
f
7-
. UJ
""CO
:•}
, .CO
uu
CO
CO
• CO
CO
;..co
i?CO
.•C 0
CO
CO
/ CO
'•CO
• CO
• CO
• zo
•: C O
,' CO
. CO
• CO
zo
.CO
CO
CO
. CO
• CO
• CO
CO
.•CO
• CO
CO
CO
UJ
ac
UJ
oe
i WARN. HOI
oeujoe
—»UJ
i WARING
NUMBER
^>
UJ
•
^
C9
' SC
0
—J
.3,
96~ 36 :
38.4 59 ;105.20 0
3
22rA 103
t4 ' cc'.K
l u j .. ..40
. t o .. -u
: J o . t 33'
jj X
XU
QX
X
0 ..:3B.4
0 ;5) .. .2^ 6
.' 64 ; 1 8 ; 0 ,38.305- 10.5-979
•5..'
-.6 •2-4
98 37 . 1 38-192 1 0 5 - 8 X 6
.
^ 6 0 .' 1 38;168 1 0 5 4 9 2 4
.7. .23 . .139
1 : 13
73 26 1 "'38.83,6. X 0 6 - 8 2 5
2 . 1 2 ; ,80 27 1 3.8-8X6 1 0 5 - 8 7 3
3 19
136 58 1 3,8 i 812 X0;6 ..2:2,6
4 20 . 13 2. 56 • 1 3 8 : 7 3 3 1 0 6 . 1 6 2
5
..181; , :83 , 1 38.732 .106.178
• .38.653 106.0 56
6
,76 ': 25 .0
7
73 .23 0 33;534 10 6.0 72
8 ;.i4 • / 1 7 5. 80 ^ 1 38.5X2 10 5.50 7
9 21
159 71 1 38.498 1 0 6 . 0 7 6
1
5
.
1
105 41 1 38.272 1 0 7 . 1 0 0
2 .,-2:7
127 53 1 38.133 1 0 7 i 7 3 6
• 3 - ,. 2 8 156 -.59 0 38.0 2X 1 0 7 . 6 7 2
,1 . 26 ,•. 9 1
33 b ;33.0X4 1 0 8 . 0 5 4
78. 26 1 39.932 .10 5.277
1 4
2 • •- 5 - 114 . 46 1 39.742 1 0 5 . 5 1 0
3 17
125 "52 I 39.0X7 1 0 5 . 7 9 3
1 .16
76. 25 I 39.x64 1 0 6 . 0 6 2
1.0 0 38
2
9
I 39.0X2 •106.891
7
89 3 2 0 39.624 1 0 7 . 1 0 6
1
.2
118 48 0 .39.552 10 7.412
6 . 123
3
51 I 39.548 1 0 7 . 3 2 0
4 - • 8 • 134 57 •3 39.233 1 0 7 . 2 2 8
5
132 56 I 39.227 1 0 7 . 2 2 4
1, 2
147 64 1 40.559 1 0 6 . 8 4 9
. 1 0 2. 39 . X 40.486 1 0 6 . 8 3 1
2 . ; 2A:
3 ,-3 ...1 1 1 - 4 4 1 40.073 1 0 6 . 1 1 3
1
100 38 . I 40.467 .107.952
1
i
r- •
! CELSIUS
TEMPERATURE = ; 3
i
. 1
NAME OF SPRING
'
%
m
i,.H-nj-uw
1 , 1N1A1T A
n
-T
i R IS
oU.PrMR
n iIi iN
i iG?O T S P R I N ••
F
R E M O N -TCITY
H
G • ,.i~
''..-^.f-s
- A I^
Iii
CANON
HTuOO
.
. '.- " V. -."/
F U L LI N VIDE R ::. WA R M S P-R ING
VALLEY VIXW HOT SPRINGS
.MINERAL HOT; SPRINGS
V<^- r:: -^^^c
CEMENT CREEK WARM SPRING
• [rv, :,
.RANG E R,: W A R M S P R I NG
COTT0.Ny.0O,D;HOT S P R I N G S MOUNT PRINCETON HOT SPRINGS
'-HORTENSE H O T S P R I N G ' '
B R O W N ' S C A N Y O N ' W A R M SPRING ( 2 )
,3R0WN S G R O T T O WARM S P R I N G ( 2 ) ;
i^i-i;. i
^
tfAUNITA H D T ^ S P R I N G S
v;
;;:.
PONCHA H O T S P R I N G S
.-,-:.--{.
CEBOLLA ( P O W D E R H O R N ) ' H O T S P R I N G S
ORVIS' ( R I D G W A Y ) . H O T ' S P R I N G -;'.•...:; '-^.''s/'^g^
O U R A Y : ' H O T .SPRINGS : ..• ,„;..;-,• . . - / " - / A :;!:r'"*/:?.';;P
LEMON- H O T S P R I N G '.• :/•
-o- -..^ ."--f^W
E L D O R A D O S P R I N G S .IDAHO S P R I N G S
H A R T S E L HOT S P R I N G S
RHODES WARM"SPRING "
CONUNDRUM HOT SPRING
D O T S E R O WARM S P R I N G S
S O U T H C A N Y O N -HOT,SPRINGS
GLENWOOD SPRINGS ;
:'•> *-?:
AVALANCHE"SPRINGS
PENNY H O T S P R I N G S
ROUTT HOT SPRINGS
S T E A M B O A T [SPRINGS ' '. :>.. \H O T SULPHUR S P R I N G S
JUNIPER H O T S P R I N G S
.
t*. • f'.
'•'\
^ air,-*.
:'
•
•
'-..'. •'
. IDAHO' ••
•
•:,'-'-
ID
ID
.10
ID
ID
• 10
• ID
. 10
.1 192
2
3 193
4.. 191
• 5'
6
7
8
9 196
ID
ID ^ 1 189 .
ID ' 2 190
ID 3
107 42
107 42
87 31
125 . 51
H
168 76
170 77
H
118 48 89 32
112 45
10 0
37
1
0
1
I
1
1
1
I
I
X
42.9X0
42.891
42.656
42.562
42.336
42.305
42.135
42.118
42.1X4
42.725
1 42.620
1 42.542
•• • v
111.555
111.702
111.607
111.801
111.719
111.708
111.930
111.929
111.264
112.873
112.014
1X2.903
/I
(WARM -SPRING)
SODA S P R I N G S
., '
(HOT'SPRINGS)
MAPLE GROVE HOT SPRINGS
WAYLAND HOT SPRINGS
SOUAW H O T S P R I N G S
BEAR L A K E H O T S P R I N G S
INDIAN SPRINGS
LAVA. H O T S P R I N G S
(WARM S P R I N G S )
.'t..^
«!••'".'•,"•• * T » » « ' ^ 7 T ^ -
TEMPERATURE =>:
<o
CO
_i
-* S *»
ca >
cc
INAME OF SPRING
'^
-^•rr.'9-o:
ID
5
ID
••/ 1 0 - 6
7
; ID
8
ID
X
••ID
2
ID
I D -3
1.9XA'' 109
75
; 76
194
195
186
.4 X82
5 18 4.
.6
r/io'
X 173
ID
2
-174
• ID
3
X7:5
ID
.4
178
; ID
.
5
ID
6 17 7
. ID
18X
7
.- I D
8
. ID
1 153
ID
2
X65
ID
3 154
ID
4 169 :
IP
, I P 5 156
6 157
ID
7 .16 9A,
•ID
1593
.8
• ID;
1
ID
1 153
ID
2
-:io
ID 3
10 . 4 1 5 2
V i o 5 .154
1 15.7.
ID
' - ID 2
1
ID
2
14 7
. .ID
1
102.
ID
2.
1
03
ID
.3
14
0
ID
'
.4
X4X
ID
ID ,5 X32
6 142
•ID
- ID 7 1 3 3
8 X43
ID
^
9
134
ID
10
135
ID
1-1
136
• ID
• ID
. ID
7fr
24 ,
25 ,
25
. 8 0 . 2.7';:,
98 V37.
29
,;8 4
'••:'•
v -
42-389 X 1 2 . 0 8 9
42-341 1 X 2 . 4 3 4
4 2-175 X12w239
42.153 1 1 2 . 3 4 9
42.053 1 X 2 . 2 4 2
42..452. X X 3 . 5 2 0
4 2.255. XX 3 . 5 7.9
42.;226 X 1 3 - 7 8 0
42.170 1 1 3 - 8 5 7
42.107 1 X 3 - 3 9 0
4210 99 1 X 3 . 6 3 5
47
116
.20 4 .95
' 9 6 . 3-6./'
12 9 ; 5 4 : Q ; 4 2 . 7 0 3 1 X 4 . 3 5 7
: X 2 9 / 5 4 - r/42.587 1X4.. 85 9
X30
55 : X- 42-&86; 1 X 4 . 8 2 6
100
3 7 - 0.-42.413 XX>.X61
36 X 42.347 X X 4 . 5 0 9
96
90
32 0 42.309 X X 4 . 3 2 3
69
20- 0: 42.015 X X 4 . 2 3 7
114
46 0- 42.0,05 1 X 4 . 5 0 4
105
41 I 42.799 1 1 5 . 7 4 4
il4
4 6 X 4 2,799 1 1 5 . 7 2 1
44 1 42.796 1 1 5 . 7 3 2
111
44 D- 4 2.779 1 1 5 . 7 1 6
111
41 0 .42.767 1 1 5 . 7 2 5
105
39 X 42.762, 1 1 5 . 7 3 9
.102
156
6 9 : 0 42.337 1 1 5 . 6 4 6
51 r .4 2 i, 030'1 1 5 . 3 6 7
.123
75
25 0 . 42.866 1 1 6 . 3 7 2
111
44 i : 43.792 1 1 1 . 4 3 5
43.653 1 1 1 . 7 1 7
W
:- ,.y1X 43.652 1 1 1 . 6 9 8
48 I , 43.643 1 1 1 . 6 8 6
12 0
25 0 43.427 1 1 1 - 4 0 5
75
32 1 43.112' 1 1 2 - 1 6 9
89
W 1 43.040 1 1 2 . 0 0 6
44
111
0 43.364 1 1 3 . 7 8 1
52
.125
0 .43.325 1 1 3 - 9 1 6
49
120
I 43.988. l l 4 . 7 9 8
51
123
1 43.984 1 1 4 . 4 8 6
38
102
1 43.802 1 1 4 . 5 8 6
37
99
1 43.779 1 1 4 . 5 3 9
W 1 43.703 1 1 4 . 7 3 9
157 70. L 43.583 1 1 4 . 4 1 0
H I 43.646 1 1 4 . 8 1 4
H 1 4 3.639 1 1 4 . 4 8 8
145 63 X 43.605 1 1 4 . 9 4 7
105 41 I 43.580 1 1 4 . 8 3 4
177 81-. X 43.561 1 1 4 . 7 9 1
DOWNATA'
HOT
SPRINGS
PLEASANTVIEW WARM SPRINGS
WOODRUFF ..HOT SPRINGS . , „.
.SEAR,S- SPRIN,G- C9) ,: , \ ;:
'/.•
(WARM-SPRING)
"":. / • ' • : " J ' - : "•::/':.:
OAKLEY WARM (HOT) "SPRING- . •
;/'•-.':
' '-^h-' •
:.:'
'v/..• '
(WELL ( H O T ) ) ( B R I D G E S P R I N G ) . (FRAZIER H S
DURfEE SPRING (9) .
,:•-;,..„, , •,:, . .•-/tC A
HOT S U L P H U R ( M I R A C L E H O T ) S P R I N G S ' " ' ^ X ' ' ' ' ' {
BANBU.^Y" HOT S P R I N G : ".'' '..,.;;
•:-•.;
ARTESIAN CITY"HOr:SPRINGS .V ; !
- : :,
NAT-SOO.-.PAH WARM- SPRING
'! ,
•* • •
THOROUGHB.^EO SPRINGS --.
MAGIC.HOT SPRINGS
BRUNEAU HOT SPRINGS"
BAT.AND PENCE (TRAMMEL#S) HOT SPRINGS
INDIAN BATHTUB HOT SPRINGS
.INDIAN -HOT..: SPRINGS
MURPHY HOT SPRINGS
PINCOCK (GREEN CANYON) HOT SPRINGS
ELKHORN'WARM SPRING
:., ...•.;.;
HAWLEY';WARM' SPRING ./. ; :'•_'>.:•:,'•.•
HEISE HOT SPRING
,/.,; ., , , ..
YANDELL SPRINGS'.-., "
(WARM SPRING)
CONDIE HOT'SPRINGS
PIERSON HOT SPRINGS
(SPRING (HOT))
RUSSIAN JOHN HOT SPRING
EASLEY HOT SPRINGS
(SPRINGS • (HOT))
GUYER HOT SPRINGS
SKILLERN.HOT SPRINGS
WARFIELD HOT SPRING
LIGHTFOOT\HOT SPRINGS
PREIS'HOT SPRING
WORSWICK HOT SPRINGS
1- .
V^r=^t.^::,f,;&.fflii>
.;'•:'• '
! ,'. :
^
•^f
VT:
TEMPERATURE ^ '
I*
CO
; <J
M
CO
S="
^_
2
NAME OF SPRING
47 1 43.556 114.413 CLARENDON HOT SPRINGS
' " ""V*
63 1 43.504 114.356 HAILEY HOT ISPRINGS
• ID 14 138
54 X 4 3.4 22 114.628 ELK CREEK"HOT SPRING ,12 9
• ID 15 1 3 7
15 0 .66
I 43.382 114.932 WALDRO? H.O,T SPRING
71
X59
0 .43.292 XX4-906 BARRON/S HOT SPRING .
• ID 1 6 - 139.
X .43.05X XX4-952. WHITE ARROW HOT SPRINGS
• ID 17 17 0 , ,143. 65
..80 .27 I 43.0.50 XI4.933 HOT SULPHUR LAKE .
• ID 18 1 7 1
115
4^6, . X 4 3.;8X8 115-863 (WARM SPRINGS)
. ID X .82
.130 5 4
2 12 3
0 .43.8X4 XX5.04 5
V ID
130 54 0 .43.802 115.393: GRANITE CREEK SPRINGS
"3 120
ID
148
65
•- : •
0 .43-789 1X5.434 DUTCH:FRANK SPRINGS
• ID 4 1 1 9 .
5 117
ID
W 0 43-779 XX5.48X POOL C.^^EEK HOT SPRING "
. • ID 6 1 1 6
168
76 X 43-754 XX5.570 NEINMEYER HOT SPRINGS ...
ID ••; 7 1 1 5
H 1 43.736 X15.58 0 VAUGHN HOT SPRING
49 I 4 3.726 11,5.602 LOFTUS HOT SPRING ""
120
- ID 8 1 1 3
ID
H 1 43;. 721 115.615 SMITH "CABIN HOT SPRINGS
9 112
141 .6X 1 43.697 115.655 SHEEP CREEK" BRIDGE HOT SPRING
- ID XO 110 ;=
84:
ID XX
154 57 1 43.669 115.698 TWIN SPRINGS ..
ID 12 12 6
12 2 49
I 43.638 115.127 (HOT, SPRING)
W I 43.6X3 115.250 ( S P R I N G S )
.. ID.X3 12 4
W 1 43.6X3 115.153
. ID 14 125
120
49 1 ,43.603 115.069 ( H O T S P R I N G )
. ID X5 127'
132 56 .1 43.553 11.5.273 P A R A D I S E H O T S P R I N G S
• ID X6 12 9
ID X7 12.8
.138 59
3 4 3.5 42 1X5.285 B R I D G E H O T S P R I N G S ( 8 )
ID X8 131 . .157 70
\
•
X 43.154 XX5.5X5 .(HOT'SPRINGS)...
• ID 19 131A
1 43.X13 XX5.305 L A T T Y HOT S P R I N G
130 55
ID 20
W X 43.0 05 XX5.X25 (WARM S P R I N G ) .
ID 2X X 3 X 3
125 51
0 .43.0 02 XX5.X7X
• ID 1 5.6
130
55
I 43.951 XI5.353 R O Y S T O N E HOT S P R I N G S
.-:I.D" 2 159
128 53
X 43.425 X16.718 G I V E N S HOT S P R I N G S
X
TD
.62 X7 X 44.X50 111.104 LILY PAD LAKE .
10 •. 2 151
U 0 .44.135 111.303
41
105
•'•io
3
0 .44.05X 111-459 ASHTON WA RM 'SPRINGS
34 29 I 44.253 112.539 (WARM' SPR INGS) .
X 1 4 8.
ID
50 I 44.X44 112.54 6 LiDY HOT SPRINGS
121
2 X50
ID
3X
87
X
1 44.6X3 113.365 (WARM SPR INGS)
. ID
65
29
2
X 44.267 113.450 BARNEY HO T SPRINGS
X08
84
ID
44.95X 114.705 (WARM SPR ING)
X
.
.54
H
X
ID
46
115
2
1
44.836 114.790 HOSPITAL HOT SPRING
ID
49
55
I
121
44.799
. ID 3
114.806 (HOT. SPRI NG)
X 44.784 114.854 COX.'HOT S PRINGS
130 54
ID ' •4' 49
149 64
1 44.730 114.'995 SUNFLOWER HOT SPRINGS
ID
5
63
I 44.722 114.017 (HOT. SPRI NG) .
114 46
ID
6
57
ID
7
wI 1 44.661 114.650 (HOT,SPRI NGS)
87 1 44.645 114.738 (HOT SPRINGS) '
56
190
ID
8
50
58
121
I 44.626 114i598 SHOWER BA TH SPRINGS
10
9
50 X 44.524 114-175 BEARDSLEY HOT SPRINGS
125
10 1 0 X05
88
0 44.511 114-880
ID l l
• ID 12 -1:4*4 ;• ID 1 3 14.5
11.6
145
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TEMPERATURE = ! :
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NAME OF SPRING
..w
1 44 .383 1 1 4 . • 0 8 9 ( W A R M S P R I N G ) r
,.v-/F " J - : , - /
X, 44 .269 1 1 4 . .754 SUNBEAM H O T S P R I N G S
, '* .. ' .•
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ID X4
:.;H .0 44 .264 1 1 4 . 844
91
• I D 15 '92
,4:4.
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./ID 16 10 0 • 1 0 5 . 4 1 . L 44 .254 1 1 4 . 443. S U L L I V A N H O T S P R I N G S
.9.0,.-.
H
.
1
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4
.
1
7
0
,4
4
.246
883
. ID
57 1 44 .243 114,. .671 ROBINSON BAR RANCH HOT SPRINGS - ,
; IP 18
95
,135
ID 19 , 94 , :;.ia5 41
X 44 .;2 2 2 1 1 4 . .931 STANLEY HOT SPRING
20
ID
99
."
121
50 . 1 44 ,167 1 1 4 . 6 25 SLATE CREEK H.OT SPRING
ID 2X 1.01
40
I 44 ^XOX 1 1 4 . 853- (WARM- SPRING) , ,
.103
ID
X 26
. 94 35
0.:44 1^9 00 1 1 5 . 496
"" ' .,'J.V'I - • - . ' ' . . • S ' 4 . . * ' .
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ID 2. ,25 . ;• 1 1 6 4 7
d 4 4 .850 1 1 5 . 691
ID 3
-15 7 '69;- 1 .44 .8 29 1 1 5 . .213 K W I S K U I S "HOT SPRING . .
: V ^ '• •'- ' C \ '}
tl 6 2 7 2 • X 44 .312 1 1 5 . 121 v C H O T j S P R I N G ) "
ID. 4 4 8
ID
5 .- - V • 1 9 1. -88 ,0 .4 4 .795 1 1 5 . 128
• ID ,.6 2 9
,, H 0 .44 .754 1 1 5 . 685
ID
7
1 1 6 - 46. 0 .44 . 7 3X 1 X 5 . 020
- ID .8 47
1 3 8 ' 58 - I 44 .7X7 1 X 5 . 016
ID -g ' 4 6 •116
46
1 44 . 7X 9 X X 5 . .2 0 7 (HOT SPRINGS)
ID 10
49 - 1 44 .675 X X 5 . 944 (HOT SPRING) ' " .:• -"--. •
28
.12 0
31
0 44 .537 X X 5 . 689 MOLLY^S HOT SPRING '
138. 59
• I P XI
30 . 121
50
' ID X2
0 44 .626 X X 5 , .756 TRAIL CREEK ; K 0 T SPRING (9)
ID .13 44
.; ,
. H X 44 .6 27 . X X 5 . X 9 6 SHEEPEATER HOT SPRINGS
ID 1 4 . .8,6
.»w 0 44 .571 X 1 5 , 071
•.ID 15
X88 .87 I .4 4 .565 X X 5 . 597 V U L C A N H O T S P R I N G S / - ^
32
ID .16 ,33 .
^'T:-';^^;•.? "
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0 44 -54 4 1 X 5 . ,312
.. ID 1 7 . .4 3 : xxo . 43
ID .1.8. .42
;. H 0 .44 -5 24 X X 5 . 28 0
ID 19 .41
.w 0 44 .443 1 X 5 . .234
'.,
39.
H X. 44 .429. X X 5 . 763. BULL:CREEK HOT SPRINGS
/ID 20
ID 21 87
w 0 .44 .399 X X 5 . 017
ID 22 35 .
H 1 44 .3 9 9 X X 5 . 820 ( H O T ' SPRINGS) .
- .
* '-'. *.23
36
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.3.91
37
834
X
X
5
.
(HOT
SPRINGS)
'
X
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ID 24 37
90 . 32
X- 44 .380 X I 5 . 843 (HOT'SPRINGS)
• ID 25
38
X86
86
X 44 .363 X I 5 . 356 BOILING'SPRINGS
ID 26
40
90 . 32
I 44 .328 X X 5 . ,801 (HQT,;SPRING)
X20
49
IP 27
X 44 .252 X X 5 . 891 (HOT SPRINGS)
ID 28
89 .
H 0 44 .203 X X 5 . 045
37
ID 29
81 . XOO
0 4 4..X57 X X 5 . 188 S A C A J A W E A HOT S P R I N G S
ID .3 0 73
76
168
1 4 4 • X53 X X 5 . 995 ( H O T . S P R I N G S )
• ID 31
80
184
85
0 44 .X53 1 1 5 . .310 B O N N E V I L L E HOT S P R I N G S
ID 32
77
141
61
0 44 .075 1 1 5 . 788
,
ID 33 7 8
W 0 44 .074 1 1 5 . 554 H A V E N LODGE ( 9 ) "
.
79
• ID 34
.148 65
0 44 • 071 1 1 5 . 541 K I R K H A M H O T S P R I N G S
IP 35
103
40
I 44 .0 60 1 1 5 . 816 (HOT S P R I N G )
;:
' -1IP 36
74
123
51
0 44 • 055 1 1 5 . 906
ID "37 75
H 0 44 .051 1 1 5 . 826
76.
130
• ID 3«
55
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• ID X3
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NAME OF SPRING
2
109
13,2
. 14 3
43
56
65
93,
il57
.121
.34
70,.
50.
0 . 4 4 - 9 7 1 116 1 9 9 - K R I G B A U M H O T S P R I N G S
X 4 4 . 8 5 3 116 4 4 4 S T A R K . E Y H O T S P R I N G S
I ' 4 4 . 6 7 9 115.231 W H I T E L I C K S , H O T S P R I N G
H 'X 4 4 . 6 6 7
,44.64X
44-582
,44-531
4 4-515
.44.5X0
44.4X5.
.44.306
;4 4 . 2 X 2
-44-185
44.090
4 4 . 3 05
-45.3X3
45.093
45.0X0
-45.357
, 4 5 . 5 02
45.343
.45.307
45.788,
45.312
45.277
45.169
45.068
IH
100. 38
. 1 5 9 •7X
1 9 7 ,92
'.,165 7 4
I
17 5 "80
: 7 1 .22
- 1 7 5 .8 0
.112
.4 5
. 1 2 5 ; ,52
H
109
43
199
13 0
1 41
112
93
.55.
60
45
136
110
116
57
43
47
148
105
118
65
4X
48
XX8
48
.45.029
45.A 29
45-4X5
45.X5X
45-039
46-465
46-463
46.223
45.462
46.316
46.133
46.005
I
H
H
H
H
116*305 ( H O T . S P R I N G S ) ,
116.045 H O T C R E E K ' S P R I N G S
116W631
116-751
116-055
116.035
116.030 CABARTON HOT SPRINGS
116.744 CRANE" CREEK.
116.710 COVE. CREEK. -116-115.
115-047
1X7-04 7 WEISER WARM (HOT) SPRINGS
XX'3.839
XX3.837 SALMON H O T ' S P R I N G S ; • XX3.608 SHARKEY' HOT :.SPRING
XX4.933 .(WARM SPRINGS)
XX4.450 (HOT, SPRINGS)
XX4.462 OWL CREEK HOT SPRINGS
XX4.335 BIG CREEK HOT.SPRINGS
1X5-X99 REP RIVER HOT SPRINGS
X15.045 BARTH HOT SPRINGS
XX5.9X4 BURGDORF HOT SPRINGS
1X5.308
XX5.827
XX5.688
116.0 0 8
116.172 RIGSINS HOT SPRINGS '
116.291
116.292 ZIM^S RESORT (YOGHANN) HOT SPRINGS
114.935 COLGATE"WARM SPRINGS
114.871 JERRY JOHNSON HOT SPRINGS
114.70 9
115.035 WEIR CREEK HOT SPRINGS
115.257 STANLEY HOT SPRINGS
115.090 STUART HOT SPRINGS
115.021 MARTEN HOT SPRINGS '
:
••-,"•.
' < . :
" • . ; • , . ' ; . .
-:
^ - . ' "
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-
MONTANA
MT 1
MT 2
MT 1, 36
HI '2
HI 3 40
HI
HI
139 60 1
76 ,25 0
.70. 2X X
44.985
44.798
45.757
45.706
45-552
111.615
111.145
110.256
XXO-975
XXO.142
HOT SPRINGS
(HOT SPRINGS) HUNTERS HOT SPRINGS
BRIDGER CANYON SPRINGS (4)
ANDERSON SPRINGS
W0LF:CREEK
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-
TEMPERATURE ^ '
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89
.121
31
32
20
30
121
125
141
161
127
27
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: 134
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... 7 5
; 14 3 . 6 5
76
/X63
77
/;170
1.1'65 ' 7 4
111
44
125
52
./• 8 5 30
' 69 2 1
. 84 28
45
112
45
114
^
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4 5 . 3 37 X X O . 6 9 2
45.088 X10.771
43.036 110.666
45.659 111.185
.45.603; 111.900
45.59X i l l . 8 9 9
45.573 111.584
4 5 . 8 96 : 1 1 2 . 2 3 3
45.690 112.282
45.46X; 112-474
45*422 112.693.
45.170 112.158
45. Xll 112.713
45.X04: 112;751
45.747 113.936
4 5 . 4 57 1 1 3 . 1 0 5
45.366" 113.410
4 5.84 5 1 1 4 . 0 3 3
45.695 114.379
45.695 114.359
46.545 110.903
4 6 . 4 4 7: 1 1 1 . 9 8 5
45.50 5 112.777
46.598 112.109
45.x99 112.095
46.180 112.788
.46.042' 112-811
4 6.729 114.530
46.x04 114;002
47.995 108.454
47.22X 1 0 9 . 4 7 4
4 7 . 5 31 1 1 2 . 8 5 8
47.507; 114.663
4 7.328 114.789
NAME OF SPRING
'T^f
CHICO HOT S P R I N G S "~''•"'•'.- •-~T'!-^
LADUKE (CORWIN) HOT SPRING './
BEAR. CREEK. SPRING
.-'. v ' '-/'.-...
BOZEMAN 'HOT SPRINGS ":
' " ' •> '";
..(.WARM" S P R I N G S ) :: ••-,.[ •"-'-• -j;';^'/':' ^/-.'C.-.
P O T O S I : HOT SPRINGS
.
./*•/• r .'.•, ,;
NORRIS HOT SPRINGS/^;
;. • . " ' ...
PIPESTONE'HOT SPRINGS
:... .- .
BARKELS (SILVER S T A R ) HOT SPRINGS : ' ;
BILTMORE HOT SPRINGS
^ '
ZIEGLER HOT SPR I N G S , „-.
/,;.•• •
PULLER HOT SPRINGS ';
..-' /
.;,CWAR^I- SPRING^ A R E A ) ,/:-v
/-,':-.. '. -V -/
•BROWN':SPRINGS
' •/;'^''-.. , ';•' "/ v
':.'''-,
GALLOGLY SPRING
, .' .-•;;.-.".'•, ;ELKHORN HOT SPRINGS
.T-/-'"" ' i:
JARDINE (JACKSON, BIG HOLE)"HOT SPRINGS
MEDICINE HOT SPRINGS ..
(HOT S P R I N G ) .;• .
,.
'•' .'^', ' /'/'•"
(HOT. S P R I N G S )
•^•'/
.. ' i-^'.-'WHITE SULPHUR S P R I N G S
ALHAMBRA-HOT SPRINGS
"/, •...'.. "
<
'
'
/{
NEVADA
90
90
73
75
110
97
88
•
HELENA (BROADWATER) HOT S-PRINGS
-BOULDER HOT SPRINGS . " - " . ' ' .
WARM SPRINGS (STATE H O S P I T A L )
GREGSON "HOT'SPRINGS :..:'
' :• .'/-',/
LOLO t&RANlTE) HOT SPRINGS /
' /.';^
SLEEPING CHILD HOT SPRINGS •
BIG .WARM SPRINGS
'v.-.'/
: (WARM .SPRING), ;
,. ^>' v ' :':. ;.••>,'-•',
MEDICINE SPRINGS
CAMAS HOT SPRINGS
•':/''/
->i-:-r
NV 1
NV 2
.NV 3
NV . 1
NV 2. 150
NV i : 151
NV 2 141
NV 1 138
NV 2
NV 3
. 5 •-
H I 35.982 XX4.748 (HOT SPRINGS)
H
35.964 114.743 (HOT SPRING)
H
35.944 114-733 (HOT SPRING)
32
36.722 114.717 MUDDY SPRING
32
36.710 114.714 (WARM SPRINGS)
25
36.564 115.659 INDIAN SPRINGS
23
36.157 115.903 MANSE SPRINGS
43
36.970 116-718 HICKS HOT SPRINGS.
36
36.963 115.725
31
36.954 115.726
-^;I — •
TEMPERATURE ^ '
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NAME OF SPRING
c/>
NV
82
4
27
NV
5
82
27
NV
6
84
28
NV
7 139
82
2 7.
NV
8
94
34
NV
9
94
34
92
NV 1 0
33
91
32
NV i i :
80 . 2 6
NV 1 2
93
33
NV 13
' 82 27
NV 14
83
28
NV 15
70
NV
21
1 144A.
88
NV
31
2: 145
14
4
70
NV
.21
3
128
NV
53
4 146,
,90
NV
32
147
1
90
NV .2 1 4 8
32
97
NV. 3 149
36
80
26
,.NV .1
76
24
NV
2
•
\
NV
3
110
43
NV
4
140
59
NV
5 112
160
NV
.71
111
6
'-70 21
NV
1 142
.70 . 21
NV
142
2
.
7 0,, 21
NV
142
3
128
NV
103A
.53
1
12
2.
•NV
2
NV
3,
22
NV
72
4 104
135
i'7
0NV
.21
5.
100
NV
37
6 134
12
8
82
NV
:27
7
129
73
NV
22
8
.99
N\^ 9 126
37
NV 10
99
37
NV. 1 1 12 7
1 6 0 171
N V . 1 2 . 136
17 5
23
NV 1375
23
NV 1 4
85
29
NV 1 5 137
92
33
NV 1 6 134A
92
33
NV
1 121
NV . 2•
•NV • 3
92 3 3
82
NV A
180
36-493" 1 1 6 - 3 4 2 .FAIRBANKS SPRING
36.433 1 1 6 - 1 4 3
36.479 1 1 5 - 3 2 3 R O G E R S S P R I N G
36.466. 1 1 6 . 3 2 5 L d N G S T R E E T S P R I N G
36.464 1 1 6 . 3 1 4 .
36.430; 1 1 6 . 3 0 4
. .
36.427 1 1 5 . 2 8 9 D E V I L S V H O L E •
36.421 1 1 5 . 3 2 3 C R Y S T A L P O O L
36.406 1 1 5 . 3 0 4
36.401 X X 6 . 2 7 2 P O I N T OF ROCKS S P R I N G S
36.391 X X 6 . 2 7 8 J A C K ; R A B B I T S P R I N G
36.375 X X 6 . 2 7 6 B I G . S P R I N G '
.37.861 X X 4 . 3 X X D E L M U E S - S P R I N G
37.807= X X 4 . 3 8 4 PANACA SPRING
37.783 X X 4 . 5 3 2 B E N N E T T , S P R I N G S
.37-622 XX'4.5X3 C A L I E N T E HOT SPRING
.37-597 X X 5 . 2 X 4 . H I K O f S P R I N G
37.531 X X 5 . 2 3 4 C R Y S T A L S P R I N G S
37.4 62; X X 5 . 1 8 8 ASH .SPRINGS
37-94 8 1 1 7 . 8 0 4
37-913 1 1 7 . 8 4 3
.37-352: 1 1 7 . 6 5 3
37.824 1 1 7 . 4 8 4 P E A R L HO T' S P R I N G S
37.826 1 1 7 . 3 4 1 ALKALI H OT SPRING
. 3 7 . 7 5 9 . 1 1 7 . 6 3 1 (HOT SPR I N G )
3 8 . 6 8 8 1 1 4 - 6 2 4 GEYSER R A N C H - S P R I N G S
3 8 . 6 7 2 1 1 4 . 6 2 5 GEYSER R A N C H S P R I N G S
3 8 . 6 5 8 1 1 4 . 5 3 0 GEYSER R ANCH S P R I N G S
3 8 . 9 5 0 . 1 1 5 . 2 2 9 W I L L I A M S HOT S P R I N G S
3 8 . 9 5 1 . 1 1 5 . 7 0 2 BIG WARM SPRING
3 8 . 9 3 7 1 1 5 . 6 9 5 L I T T L E W ARM S P R I N G ,
3 8 . 9 2 4 . 1 1 5 . 0 8 1 PRESTON SPRINGS
3 8 . 5 2 2 1 1 5 . 0 5 1 EMIGRANT SPRINGS
3 8 . 5 9 4 1 1 5 - 1 4 0 MOORMAN SPRING
3 8 . 5 6 2 1 1 5 - 5 3 0 BLUE EAG LE S P R I N G S
3 8 . 5 5 5 1 1 5 - 5 3 2 KATE 'SPR ING
3 8 - 5 5 5 1 1 5 - 7 7 1 BIG, (LOCK E S ) S P R I N G
3 8 - 5 5 3 1 1 5 - 7 6 1 HAY CORR AL SPRING
3 8 - 4 65 1 1 5 - 7 9 1 C H I M N E Y S P R I N G S
3 8 - 4 . 4 2 1 1 5 - 0 1 4 B U T T E R F I ELD S P R I N G S
3 8 . 4 2 3 1 1 5 . 0 2 4 F L A G ' S P R INGS
NG
3 8 . 4 0 0 1 1 5 . 8 5 8 STORM SP
HOT
CREE
K SPRING
38.381 115-154
MOON RIV ER S P R I N G
38-350 115-181
FISH SPR
33.758 115-435
INGS
UPPER WA
38.694 115.436
RM S P R I N G AND (WARM
UPPER WA
RM. S P R I N G
38.533 116.464
(HOT SPR
ING)
38-520 115.365
''-f
SPRING)
I-l..— l.l'JI '
'.
\
•'vfim-f. - • . * , !
I
TEMPERATURE = f
I*
.
- O
UJ
I—
VJ
"= O
|_
UJ
:f e>
«c
c:>
3 > —J
_j
—1
? s
» ae
Z
NAME OF SPRING
CO
NV
NV
NV
NV
NV
NV
NV
NV
NV
NV
NV
NV
NV
NV
NV
NV
NV
NV
NV
NV
NV
NVNV
NV
.NV
NV
...NV
• NV
NV
;;NV
' NV
NV
• NV
• NVNV.
NV
N.V
•N.V
NV
NV
• NV
NV
NV
NV
NV
• NV
' NV
NV
5
6
7 125
1 116
2 118
3 123
1 108
2 113
3 109
4
5 110
1
50
2
51.
3
4
1
141
80
206
144
101
101
159
141
H
84
28
;65
79
24
28
34
21
2
3
;4
5
6
1
,2
3
1
3
4
5
6
7
W X 3 8. 33 8; 116.660
W X 3 8 . 2 5 3 116-823
1 3 8 . 1 8 7 XX6-373
61
X 38;955 XX7-049
26
97 X 3 8 . 8 2 0 I17-X81
• W 0 3 8 . 4 5 8 117-30 3
w 1 38.965 1X8-690
62 1 38.921 XX8-200
38 D 3 8 - 4 9 4 ; 1X8;967
H 0 3 8 . 3 9 2 X18-105
38 , 1 .38.34 2 118.106
3 8 . 9 7 8 119.833
71
:;3 8.,9 0 1 119.413
61
H
W
91C
93A
.8
9 .'•93B
1 0 :;/8i5 1 1 119
12
70
1
2 .85
3 114
74
103
30
41
82
72
' H
23
40
: y
152
161
112
133
6 7
72
45
59
2.0 4,
185
95
8 6
H
H
1
2
3
4
5
6
7
1
-2
71A
73
74
75
74A
52
53
X6X
70
193
.178
72
21.
90
,81
H
190
12 0
88
48
W
38-860
38.769
,39.917
39.891
39.667
39.547
39.415
39.284
39.817.
39.422
39.0 72
39-988
39.943
39-941
39-905
39.893
39.836
39.553
39.529
39.404
39.328
39.079
39.030
39.950
39.309
39.025
.39.863
39.795
39.629
39.565
39.336
39.281
39.208
39.944
39.845
119-175
119.174
114.66 9
114.898
114.809
114.917
1X4.780
X14.365
115.611
115.683
115.635
116.043
1X6.074
XX6.68X
1X6.59X
XX6.650
XX6.067
XX6.365
XX6.389
XX6.344
XX6.858
XX5.639
XX6.655
XX7-935
XX7.553
XX7.X36
118.012
118:064
118.175
118.853
118-630
118-419
118-721
119-509
119-713
(WARM' SPRING)
(WARH"SPRING)
WARM, "SPRINGS
CHARNOCK (BIG BLUE) SPRINGS
DARROUGHS'HOT SPRINGS
INDIAN SPRINGS . .
DOUBLE_SPRING
WEDELL HOT SPRINGS
MINA HOT SPRING (7)
WALLEYS HOT SPRINGS
NEVADA':(HINDS) .HOT SPRINGS
( H O.T/S P R I N G ) : ,'"" • ". . . r . .
WILSON.HOT
SPRING
JOHN "SALVI^S'HOT S P R I N G
M O N T E NEVA HOT S P R I N G S
MCGILL SPRING •
LACKAWANNA
SPRINGS
M O O R E S RANCH S P R I N G S
SULP.HUR S P R I N G
BIG, B L U E SPRING
S I R I . ' R A N C H SPRING
SHIPLEY HOT SPRING
(HOT, SPRINGS)' ;
WALTI H O T ' S P R I N G S
L I T T L E HOT S P R I N G S
SULPHUR
SPRING
(HOT;-SPR I N G S )
(WARM "SPRING) •
.
B A R T H O L O M A E ( C L O S E ) HOT
SPENCER.HOT
SPRINGS
P O T T # S RANCH HOT S P R I N G
D I A N A S PUNCH BOWL
(HOT.SPRINGS)
(HOT^ S P R I N G )
D I X I E HOT S P R I N G S
MUD S P R I N G S
BORAX SPRING
SAND,'SPRINGS
LEE. HOT S P R I N G S
(SPRING)
(WARM)
.
(7)
"
' ..
- ,
"
SPRINGS
(10)
• * •^'^''^'^-.^ • •
''-^•^ * . ' , ' ! ; *
w:-.*.
"-
'
" : ' . .
•
-
'
-
-
.
•
'
.
•
•
•
•
*
:
•
-
'
*
'
*
Li
TEMPERATURE = ; :
t*
co
_i
5 ,«
oe
<j
NAME OF SPRING
'•-'3'^f ••
.•NV -.3 7 2
203 . 98 1 39.787 119-009 BRADYS HOT SPRINGS
NV 4
186. 86 0 3 9 - 5 9 7 119.110
.- . • •
NV ; 5 ^
91„ 33 0 39.511 1 1 9 - 9 0 8 LAHTQN H O T SPRINGS
,,. NV 6 55A
H I 39.486 119.804 MOANA SPRINGS
NV..7., 55B
94 34 D 39.421 119.767 HUFF;AKER SPRINGS
•NV ,8"
204 96 1 3 9 . 3 9 5 119.748 STEAMBOAT SPRINGS
• NV. .9 56 : 204 96 1 39.384 119.742 STEAMBOAT ^SPRINGS
, NV 10- 57- 114 46 0 39.283 119.843 BOWERS MANSION HOT SPRING
NV 11: .59
120 48 I 39.195 1X9.749 CARSON HOT.SPRINGS ,. .
NV X2 .
H I 39.167 XX9.154 (HOT) ""•;"*"':;
"
." •"., •
•NV X3 ' 62
206 97 X 39.X6X XX9.X83 WABUSKA HOT: SPRINGS "
NV X4 59A
W 0 .39.X59 X19.737 NEVADA STATE PRISON
NV 15 .,...,.
• H-1 39.05^ 119.743 (HOl/SPRING)" :
NV. 16
H I ,39.055 119.809 HOBO' HOT SPRING •"
NV 1 30C . 73 22 1 40.967.114.509 BIG. SPRINGS
NV .2
..... • 65 18 l.;40.957-114.748: . ,
••
NV 3
86 29 1 4 0 . 9 4 7 114.751 (SPRINGS)
'^ :...;.--.
NV .4 94
92 33 1 40.086 114.643 COLLAR AND ELBOW SPRING
. NV
1
,
. w 0 40*971 115.012
• NV
2
32
"92
33
NV
3
33
W
NV
4
34
65
18
•NV
5
199
93
NV
6
34A
1 4 3 = 55
NV . 1 . 75 . . 8 3
28
NV
2
3 1 ,
98 .. 3 6
NV
3
77
W
•NV
4
174 . 7 9
NV
5
.
W
.;NV; S - '
130
55
NV. - 7
88 ; 136
57
• NV
8
77A . .208
98
NV
9
• H
• N V 10
88A
129-54
NV 1 1
89 .
78 . 2 6
NV 12
186/85
NV13.
90.
102
38
NV 1 4
99A
1 5 2 . 56
•NV 15 "82
102
38
NV 1 6
91
73 : 25
NV
1
18
93
33
NV
2 . 19
165
74
• NV
3 .19
114
46
•NV
4
19A
135
58
1-40-820.115.774
1 40.782 115.361
I 40.755,115.034
I 40.585 115.284
I 40.253 115.407
0 4 0.91,7 1 1 6 . 9 0 6
1 40.762 115.040
I 40.745 116.686
0 40-597 116-130
1 40.582 116.155
1 40.671.116.837
0 40.603 116.466
1 40.559 116.591
0 40-429 115-505
I 40.400.116.517
1 40.324 116.058
1 40.318 116.434
0 4 0 . 2 9 8 116.057
1 40.222 116.065
I 40.189 115.805
1 40.079 115.035
1 40-990 117-767
1 40.962 117.491
1 40.952 117.491
I 40.923 117.108
NV
NV
•NV
• NV
L
1
1
1
5
6 •19F
7 19G
-6 64
82 27
94 34
184 85
204 96
40.872
40.831
40.761
40.602
117.936
117.306
117.491
117.646
.::;
'~i
/
;
,
.
HOT HOLE" (ELKO HOT SPRINGS)
(WARM SPRING)
(WARM SPR I N G S ) -'
-• SULPHUR H O T ' f H O T SULPHUR) SPRINGS
(SPRINGS'XHOD):
IZZENHOOD RANCH SPRINGS
(HOT^SPRINGS).}"./" . / ; . : .
WHITE HOUSE SPRING
"
- ^
(WARM SPRING)
(HOT.."SPRINGS) "
. '
:
HORSESHOE RANCH SPRINGS
BEOWAWE HOT,SPRINGS (THE GEYSERS)
^ /^'^ "', f " ' : :
; .-^
HOT SPRINGS POINT
(HOT SPRINGS).
(HOT,SPRING)
• BRUFFEY#S HOT SPRINGS
(SPRING)
FLYNN RANCH SPRINGS
(SPRING)
(HOT SPRING)
. GOLCONDA HOT SPRING
HOT POT (BLOSSOM HOT SPRINGS)
(SPRING)
BROOKS SPRING
(HOT S P R I N G S ) '
LEACH HOT SPRINGS
: r:/f-v''
/./
\ {
' "
•
•:'''-J-i-*&-^'-J-j>;-a?i-Ri*-«..';--:^!-r.-:;-;-i.4';^^
. >'..-J ;,:•-.<:::.-^..>•A-i<!;^.i-••.•-•i^.•c<•sr*;«^••i;->^i^Wl;^»;^ ^.-.^sf.
TEMPERATURE = •
lUJ
tJ
—T
CO
-J
S? UJ
K
;'v;
UJ
aE ^
0£,c>
NAME OF SPRING
CO
' NV 9
• NV 10
• NV
NV
NV
.. NV
NV
• NV
.• NV
NV
NV
NV'
NV
NV
• NV
-•NV
NV
• NV
NV
• NV
. Mv
NV
NV
• NV
NV
NV
NV
NV
NV
• NV
NV
NV
NV
NV
NV
• NV
• NV
NV
NV
NV
NV
NV
NV
NV
NV
' NV
• NV
NV
11
12
13
14
15
16
17
18,
19
20
21
1
2
3
4
5
6
7
8
9
10
11
12
1
2
3
4
5
6
7
8
9
10
11
12
13
14
1
2
3
4
5
6
7
"1
-2
56
78
79
80
68
69
16
37
53
41
38
39
50
,4 9
48
23
24
25
2 2B
27
30A
30
22
21
30D
28
17 0
174
110
127
128
129
84
199
120
103
175
134
193
175
84
186
83
193
165
186
82
20B
73
85
109
110
139
84
138
112
82
141
121
104
110
12 9
154
122
29
193
H 0" 4 0.416 117.
I 40.405 117.
1 40.366 117.
I 40.314 117.
1. 4 0.199 117.
I 40.192 117.
I 4 0.132 117.
1 40.176 117.
1 40.087 ,117.
I 40.081. 117.
1 .40.035- 117.
H 1 40.031 117.
79 I 40.0 05 117.
57 0 .40.971 119.
90
0 40.950 , 11.9.
80 I 40.858 119.
29
0 .40.826 119.
86
1 40.770 119.
28 0 40.687 119.
90
1 40.664 119.
75 0 4 0.65 0 119.
86 1 40.260 119.
27 1 40.220 119,
98
1 4 0.145 119.
22 I 4 0.104 119.
30 1 41.978 114,
1 .41.968 114.
43 i 41.927 114.
43 1 41.883 114.
50
0 41-791 114.
28 0 41-567 114.
H 0 41.424 114.
58 1 41.412 114.
45 1 41.382 114.
27 0 41.363 114.
61
1 41.183 114.
50
1 41.160 114.
H I 41.146 114.
U 1 41.068 114.
39 1 41.877 115.
1 41.776 115.
43
I 41.547 115.
54
I 41.574 115.
57
1 41.260 115.
49
H 1 41.192 115.
41-174 115.
H
41-469 115.
90
,41.150 115.
77
79
43
53
53
54
29
93
48
40
415
835
324
067
104
110.
101
494
725
605
596
644
720
007
003
328
532
113
594
365
375
380
201
683
887
378
573
071
116
735
427
75 0
677
165
072
991
986
991
993
628
924
768
184
306
290
280
14 8
734
•
- - •
• ,
I-
•
.
V:'
wr:\:
KYLE HOT SPRINGS
BUFFALO VALLEY HOT SPRINGS
HOUND SPRINGS
(HOT SPRINGS)
.(HOT SPRINGS).
CHOT SPRING)'
SOU HOT SPRINGS /
MCCOY,SPRINGS
(HOT. SPRINGS).
HYDER HOT SPRINGS
FLY RANCH.HOT SPRINGS
.•*.//.
BUTTE SPRINGS (TRE30 HOT SPRINGS)
WALL SPRING
. :^
' '-' '^••
GREAT BOILING SPRING (GERLACH.HOT SPRINGS
MUD SPRINGS
BOILING SPRING
.-" • /
(HOT SPRINGS)
FISH. SPRINGS •
(HOT SPRING)
,
(WARM SPRINGS)
.
NILE SPRING
GAMBLES HOLE "
MINERAL (SAN JACINTO) HOT SPRINGS
(SPRINGS
(SPRING
(HOT))
(HOT))
:.;^
(HOT SPRINGS)
HOT SULPHUR (SULPHUR) SPRINGS
(HOT SPRINGS)
(SPRING)
(HOT SPRINGS)
RIZZI RANCH HOT SPRING (7)
(HOT SPRINGS)
HOT CREEK SPRINGS
(HOT SPRINGS)
(HOT SPRING)
(HOT SPRINGS)
HOT SULPHUR SPRINGS (TUSCA.RORA)
HOT LAKE
I
1
TEMPERATURE 5 :
t*
r. . UJ
—<UJ
CO
=>
S UJ
s; » !
? 2
IJ
—I
UJ
o
CO
• NV 1
NV 2
- NV 3
NV
1
• NV 2
.'•NV 3
NV 4
NV 5
NV 6
^•NV
7
NV- 8
'•NV 9
,NV 10
• NV 11
• NV 12
NV 13
NV 14
NV 1
.NV 2
NV 3
NV 4
NV 5
NV 6
NV 7
NV 8
NV 9
NV 10
NV 11
NV. 12
11
19D
2
35A
35C
, 8
14
15
16
17
18
19
20
21
22
23
36
12
24
25
1
oe ,
^c
3i .
41.424
.41.064
.70 21
41.031
U
41.932
129 54 .
41.921
177 81
41.913
41.752
112 44
41.725
103 42
132 56, " 41.718
41-717
132 56'
41.703
80 26
41.565
150 56
4,1.526
104 39
199 , 93
.41-369
195 91
4X-3 65
: 73 23
41.253
17 0 75
41.050
W
41.790
U
41,745
41.730
83 28
21
41.590
71
41.395
84 . 29
45
41.393
ll2
54
41.382
129
58
.41.370
136.
41-358
132 ,, 56
41.355
109 43
41.355
73 23
41.344
127 53
41-337
78 26
41,333
71 22
41-332
102 39
41.319
75 24
H -41.175
152 67
41.146
80 26"
41.137
121 50
41.113
175 30
41.0 49
114 46
41.029
161 72
41.019
172 78
41.011
204 96
41-003
136
58
H
• ::,NV 13
NV
NV
• NV
NV
NV
NV
NV
• NV
NV
NV
NV
NV
^ •
I
•
NAME OF SPRING
117-391
117.085
117.326
118-807
118-30 4
118.707
118.840
118.919
118-523
118.504
118-298
118.562
118.570
ll8.791
118-810
118.934
118.715
119-108
119-795
119.787
119.854
119.169
119.193
119.189
119.189
119.192
119.220
119.114
119.192
119.170
119.221
119.199
119.207
119.957
119.020
119.135
119.004
119.0 29
119.018
119.015
119.012
119.007
THE HOT SPRINGS
(WARM SPRINGS)
BOG HOT SPRINGS
8ALTAZ0R HOT SPRING
(WARM..SPRINGS)
WEST SPRING
HOWARD HOT" SPRING
(SPRING).
DYKE HOT SPRINGS
(SPRING)
.." "
'..'>/
PINTO.HOT SPRINGS (EAST)
PINTO HOT SPRINGS (WEST)
CAIN "SPRINGS
MACFARLAND HOT SPRING
(WARM SPRING)
(WARM SPRINGS)
HILL;^S WARM SPRING
TWIN SPRINGSSOLDIER MEADOW
SOLDIER MEADOW
SOLDIER MEADOW
SOLDIER MEADOW
SOLDIER MEADOW
SOLDIER MEADOW
SOLDIER
SOLDIER
SOLDIER
SOLDIER
SOLDIER
MEADOW
MEADOW
MEADOW
MEADOW
MEADOW
DOUBLE HOT SPRINGS
NEW MEXICO
•NM
-NM
1
I
38
125
• 92
52
33
I 52.501 1 0 6 . 9 2 5 RADIUM S P R I N G S
X 32.795 X07.275 DERRY WARM SPRINGS
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CO
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NAME OF SPRING
CO
NM 2 -.34 : X44 5 2 I 32-753 107-334 MIMBRES KOT SPRINGS .
NM 3
. . 6 6 18 1 32.703 107.759 GOAT SPRING
. NM 4
72 22 0 32.593 107.811
NM 5 36
131 54 1 32.554 107.994 FAYWOOD HOT SPRINGS
NM
1. . \
.77. 24 0.32.975 108-631
NM 2
73 25 1 32.384 108.357 ALLEN SPRINGS
-.
..
NM 3
68 19 X 32.867 X0B.698
NM , 4.'
72 22 X 32.8X5 108-412 ASH SPRING
.; NM ,5 3 5 '
W 0 . 3 2 . 5 3 9 1 0 8 . 1 2 4 A P A C H E .TEJO W A R M S P R I N G
NM .6
W 1 32.562 108.027 KENNECOTT WARM SPRINGS ( 6 )
N.M 1
69 .20 I 32.899 109.035
-: :' ,
NM 2
69 2 0 - 1 32.330 109.044 GOAT CAMP SPRING
.NM 1
; 70 .21 . 1.33.813 106.971
.
/ ,
• N M r .'
66 18 1 33.911 107.159 SAWMILL SPRING
, NM 2 24... 83 28 I 33.572 107.600 OJO CALIENTE
NM 3.
, 87 30 I 33.279 107.563 (W ARM' SPR INGS)
. NM 4 37
109 42 0 33.129 107.254 TRUTH OR CONSEQUENCES (LAS P A L O M A S ) H.SPG
NM 1 . ,
70 21 . 0 33.898 108.501 ARAGON SPRINGS
NM 2 .
98 36 1 33.829 108.797 (UPPER) FRISLO HOT SPRINGS
• NM 3 , .
H O 33.305 108.247
. NM 4
91 32 0 33.304 108.330 THE MEADOWS (WARM SPRING) (5)
NM 5
31 27 0 33.283 108.254 (NO NAME SEEP) (6),
/
, NM 6
94 34 0 33.261 108.233 (NO NAME SPRING) (5)
\
•NM 7 25
121 49 I 33.244 108.880 LOWER FRISCO (SAN FRANCISCO) HOT SPRINGS
NM 8
H 1 33.237 108.880 (HOT SPRINGS)
•NM" 9 27
150 '65 0 33.218 108-237 (NO NAME SPRING) 15)
•NM 10. 30 , 154 68 1 33.X99 X03-205 GILA HOT SPRINGS
. "
NM XX 3X
X26 52 0 33.X92 108.180 LYONS HUNTING LODGE HOT SPRINGS (6) .
NM 12 32
113 44 I 33.162 108.209 (SPRING (HOT))
.:NM 1 3 29
.
H O 33-113 108.486
• NM 1 ,
92 33 0 33-708 109.025 F.^IEBORN CANYON SPRING
NM 1
69 20 0 34.995 106.454 CLEAR WATER SPRING
NM 2
70 21 0 34.264 106.883
NM 3
68 19 I 34.116 106.980 OJITOS SPRINGS
NM 4
70 21 • I 34.049 105-939 COOK SPRING
NM 5 23
92 33 1 34-038 106.940 SOCORRO SPRING ANO SEOILLO SPRING
NM 6
79 . 26- I 34.032 105-777 OJO OE LAS CANAS
NM 1 .
68 19 0 3 4 . 9 1 6 107.143
NM 2 2 2
73 22 1 34.903 107.085 EL OJO ESCONDIDO
NM 3
73 -22 0 34.686 107.090
NM 4
80 26 1 34.854 107-088 (SPRING (SALT)) LAGUNA PUEBLO SPRINGS (4)
NM ,5
2
75 24 I 34.347 107.091 (SPRING (SALT))
. NM 6
3
82 27 1 34.833 1Q7.091 (SPRING (SALT)) LAGUNA PUEBLO SEEPS (4)
NM
7
68 19 0 34.815 107.388
NM 8
86 29 1 34.808 107.091 (SPRINGS (SALT))
NM 9 .80 26 0 34.791 107.091
NM 10
73 25 1 34.769 107.085 (SPRING (SALT))
NM 11
.71 21 1 34.698 107.129 (SPRING)
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CO
NAME OF SPRING
CJ-:
NM 1 2
NM 1
NM 2
NM 1
. NM 1
NM • 2
NM 3
NM 4
NM 5
NM 6
•NM 7
NM 8
: NM 9
NM 1 0
•
21
72
71
72
.22
21
22
20
137 5 8
11
101..^38
10 . 1 2 0 . 4 8
12
153 69
111 43
14
90 32
13
1 1 8 47
15
163 73
16
70 21
. 1 7 :125 50
19
68
19
0 34.326
0 34.912
0 34.158
1 35.654
X 35.971
1 35.939
1 55.90.7
'l 35.848
1 35.821
I 35.793
1.35.769
I 55.601
0 35.592
1 35.548
NM 11 18 •. 85 -29 0 35.540
NM 12,
68 19 ,0 35.308
NM 1
.-.72 22 :,X35.060
NM X,
99' 37 -0.36.523
NM 2
XOO , 3 7 . X 56.508
NM 3
95 ,34 1 36.324
NM X
83 28 I 36.368
NM 2
8
113 .44 l 36.305
NM 3
H Q 36.245
•• •'
OR 1 35
OR 2 35C
OR 3 86
OR 1 65
OR .2 56
OR 3 57
• OR 4,,
•OR 5 68
OR 6 69
• 0,^ 7 70
OR 8 7 1 ,
OR 9 72
OR 1 48
OR 2 48A
O.R • 3 49
OR 4
•OR
5 49A
OR 6 49B
•OR .7 •49C
OR 8 49D
OR S 50
. - \OREGON
107.095
1 0 8 . 9 5 1 OJO C A L I E N T E
10 8 . 3 1 9
/
/ '
'
- '
105.292 MONTEZUMA (LAS V E G A S ) HOT SPRINGS
106.561 SAN. ANTONIO. WARM SPRING
105.644 SAN ANTONIO (MURRAY) HOT SPRING
106.614 SULPHUR SPRINGS
106.629 SPENCE HOT SPRING
106.628.MCCAULEY HOT SPRING"
X06.685 SODA DAM HOT SPRINGS
105.691 JEMEZ SPRINGS
106.860 PENASCO (PHILLIP S) SPRINGS
106.753 INOIAN SPRINGS .
106.827
S A N Y S I D R O WARM S P R I N G S
10.6.854
106.471
107.X33
105.7X3
105.722
105.605
106.059
105.055
105.826
SAN YSIDRO HOT SPRINGS
ALAMOS" SPRING
(NO NAME SPRING) (6)
MANBY (MAMBY S»AMERICAN) HOT'SPRINGS
PONCE DE LEON SPRINGS (HOT SPRING)
STATUE SPRING (6)
OJO CALIENTE (JOSEPH S HOT SPRINGS)'
AGUA CALIENTE (6)
-. \ : : . ' \
120 49 0 42.977 117.061 CANTER S HOT SPRING
93 34 0 42-534 117.181
.125 52 1 42.078 117.750
80 27 1 42.891 118.897 HOGHOUSE HOT SPRINGS
82 28 0 42.837 118.859
89 32 1 42-823 118-901 (WARM SPRINGS)
206 97 1 42.677 ' 118.345 MICKEY SPRINGS.
168 76 I 42.544 118.530 ALVORD HOT SPRINGS
204 .. 96 1 42.340 118-599 (HOT SPRINGS)
96 36 1 42 - 323 118.602 BORAX LAKE (HOT L A K E )
100 . 3 7 . 1 42.254 118.311
125 52 0 42.190 118.383
114 46 0 42.543 119.572
103 40 .1 42.501 119.593 ANTELOPE HOT SPRINGS
.
H 1,42.472 119-710 HART MOUNTAIN HOT SPRINGS
71 22 I 42.303 119.875 MOSS RANCH
154 68 1 42.300 119.778 FISHER HOT SPRINGS
82 28 1 42.290 119.869 MOSS RANCH
1 7 2 78 1 42.230 119.884 CRUMP (CHARLES CRUMP S S P R I N G )
197 92- 0 42.220 119.877 WARNER VALLEY RANCH'
159 71 0 42.175 119.858 ADEL HOT SPRINGS
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TEMPERATURE I '
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NAME OF SPRING
CO
OR 1 0
51
OR 11
50A
OR 1 2
37
OR
1
: OR 2
38
. OR 3
4 .40 A
OR
5
;0R
6
'OR
40
7
40E
OR
8
41
'• OR
9
42
•OR
4 4E
OR 10
OR il 4 40
OR 12 31
45
• OR 13
14
46
OR
15
47
. OR
OR
1
OR
2
, OR
3
OR
4 28
OR
5 28A
OR
6 28B
7 30
OR
8 29
OR
- OR . 1 25
1 77
•OR
2 76
• OR
3 79
.:0R
OR. 4 80
OR .5
OR ' 6 82
OR
7
OR
8 84A
• OR
1 74
OR' 2
. OR 3 51A
4 54
OR
5 84
• OR
• OR • 5- 53
7 55
OR
1
OR
2 52
OR
3 52B
OR
4 52D
OR
•OR • 5 52E
-6
OR
159 .71
112 45
159 71
66 19
64 18
67 20
65 19
66 19
66 19
67 20
75 24
109 43
67 20
67 20
204
161
190
94
.70
-70
165
66
78
75
141
103
205
157
143
195
71
105
139
71
143
145
172
107
84
82
71
59
71
0
1
0
0
a
a
6
0
0
0
0
I
X
I
H I
96 I
72 1
88 1
34 3
2X 0
21 0
74 3
19 a
26 0
24 I
51 1
40 0
97
70 0
62 a
90 1
1
H 1
22 0
41 I
H 0
60
W
22
62
53
73
42
29
28
I
22
21
22
42.078
42.077
4 2.0 73
42.998
42.997
42.990
42.980
42.960
42.952
42.929
42.923
42.725
.42.380
42.324
42.266
42-220
42.160
42.153
.42.420
42.185
42.181
42.174
42.163
42.158
42.132
42.115
42-211
43-983
43-394
43-763
43-738
43.728
43.701
43.299
43.212
43.943
45.775
43.662
43.643
43.467
43.440
43.393
43.950
43.538
43.531
43.501
43.4 81
43.274
119.882
119.933
119.922
120.770
120.653
120.723
120.780
120.655
120.639
120.645
120.801
120.647
120.331
120.327
120.991
120.367
120.343
120.346
121.950
121.823
121.807
121.517
121.574
121.62 9
121.218
121.287
122.729
117.232
117.503
117.160
117.178
117.203
117.191
117.386
117.514
118.133
118,043
118.738
118.255
118.200
118.541
118.307
119.635
119.084
119.079
119.093
119.077
119.313
.
HOUSTON HOT SPRINGS
HALLINAN
HALLI NAN
ANA RIVER SPRING •
BUCKHORN CREEK SPRINGS
THOUSAND SPRINGS
LOST CABIN SPRING
PARDON.WARM SPRING •
SUMMER LAKE HOT SPRING
BEAN -HOT SPRING ".;
WHITE .ROCK'RANCH HOT: SPRING.
ROBINSON SPRING'
HUNTE.^S HOT SPRINGS
LEITHEAD HOT'SPRINGS (JOYLAND PLUNGE)
BARRY RANCH HOT SPRINGS
HARDBOARO SPRING (3)
OLENE GAP HOT.SPRINGS
HIGH BROS (TAYLOR) WARM SPRING (3)
CRYSTAL SPRING
«ILKERSON S HOT SPRING
BIG HOT SPRING (OREGON HOT SPRINGS)
JACKSON HOT SPRINGS,.,.",.
VALE HOT SPRINGS
MITCHELL BUTTE HOT SPRING
DEER BUTTE HOT SPRING
SNIVELY HOT SPRING . .
S BLACK WILLOW SPRING
(HOT SPRING)
BEULAH HOT SPRINGS
(WARM SPRING,)
(HOT SPRINGS) '
CRANE HOT SPRINGS
(HOT SPRINGS)
(WARM SPRINGS)
HILLPOND SPRING
GOODMAN SPRING
ROADLAND SPRING
BAKER SPRING
DOUBLE 0 RANCH
^.':;* v;-
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TEMPERATURE =;
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NAME OF SPRING
? ^
"OR
OR
OR
OR
.OR
OR
OR
OR
OR
OR
OR
: OR
.OR
OR
OR
OR
OR
OR
.^•OR
OR
. OR
OR
OR
• OR
OR
:0R
/•OR
OR
• OR
.:0R
OR
• OR
OR
• OR
• OR
OR
• OR
. OR
OR
OR
OR
• OR
OR
• OR
OR
OR
OR
OR
7
8
9
10
11
12
13
14
15
16
1
1
2.
•1
2
3
4
5
1
.2
3
4
5
6
1
2
3
4
1
2
3
.4
1
2
3
1
2
3
4
12:
3
4
5
1
2
• 3
4
58 •
50
53A
61
62
520
520
54
32
:33
21
22
23
26
24
17A
17B
17
73
78
75
14
16
15
13
7
.7
6
5
18
19
20
10
11
12
8
9
73
73
69
71
67
69
10 3
92
108
.154
87
69
141
93
16 3
114
23
23
21
22
20 .
21
42
33
42
68 "
3 0/
21
51 -.
37
73
46 ,
. 'W^
105 4 0 135 58
. 80 27
80 27
H
154 73
183 87
120 49
. &9 21 '
135 58
102 39
105 41
H71 22
114 46
125 52
125 52
197 92
136 58
159 71
17 4 79
111 44
I
84 29
175 80
f
139 6 0
93 54
14.1 61
100 38
82 28
43.272
43.267
43.260
43.261
43.249
43.235
43.209
43.205
43.196
43.177
43-877
43-731
43-717
43-809
43.710
43.689
43.451
43.294
44.930
44.778
.44.550
44.201
4 4.041
44.022
44.653
44.373
44.35 6
44.286
44.894
44.448
4 4.0 71
44.002
4 4.866
44.360
44.785
44.934
44.193
44.154
44.103
45.505
45.295
45.243
45.202
45.019
4 5.741
45.150
45.125
45.060
119.346 DOUBLE 0 SPRING
119.295 BASQUE SPRING •
119.019 DUNN SPRING
119.279 JOHNSON SPRING
119.257 HUGHET SPRING
119.057.
119.141
119.06-3
119.131
119.060
120.026
121.255' PAULINA SPRINGS '
121.205 EAST.' LAKE HOT SPRINGS
122.305 WALL;CREEK HOT SPRINGS
122.292 MCCREDIE SPRINGS
122.375 KITSON SPRINGS
122.145
122.367 UMPQUA,WARM SPRINGS
117.933 RADIUM HOT SPRINGS .
117.809 SAM .O'.SPRING . .,.
117.425 NELSON' SPRING
117.466 JAMIESON HOT SPRINGS
117.022 MALHEUR 3UTTE SPRINGS
117.462 NEAL, HOT SPRINGS '
118.831 HOT SULPHUR SPRING
118.739 LIMEKILN SPRING (2)
118-575 BLUE MOUNTAIN HOT"SPRINGS
118-954 JOAQUIN MILLER RESORT
119.142 RITTER HOT SPRINGS
119.109 MT VERNON HOT SPRINGS119.427 BRIS30IS RANCH SPRINGS (2)
119.655 WEBERG HOT SPRING
121.224 (SPRINGS)"
121.201 KAHNEETA HOT SPRINGS
121.972 BREITENBUSH HOT SPRINGS
122.175 BAGBY'HOT SPRINGS
122.049 BELKNAP HOT SPRINGS
122.100 FOLEY.SPRINGS
122.240 COUGAR RESERVOIR HOT SPRING
117.971
117.805 COVE SPRINGS
117.965 HOT LAKE
117.910
117.524 MEDICAL HOT SPRINGS
118.232 BINGHAM' SPRINGS
118.661 LEHMAN HOT SPRINGS
118.732 HIDAWAY SPRINGS
116-456 WARM MINERAL SPRING
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TEMPERATURE =!:
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CO
OR
OR
OR
OR
1
1
2
1
1
2
4
^
r;
2
S Ss
193
80
186
a«=
90
27
86
i".
H-
3
I 4 5.6 31
0 45.373
I 45.293
X:45.021
3
NAME OF SPRING
XX9.704
121.697 MOUNT HOOD. FUMAROLE
121.731 MOUNT HOOD WARM SPRINGS
122.011 AUSTIN (CAREY) HOT SPRINGS
/
•r SOUTH DAKOTA
SO 1
SD 2
SD ,3
SD 4
4
2
1
3
/
TX.
TX
TX
TX
1
1
1
2
". _
3
1
2
72
90
89
68
22
32
31
19
103.376
103.509
103-483
103.551
TEXAS '•"-•••:
/
105
114
100
126
0 43.525
1 43.447
I.43.438
I 43-335
40
45
37
52
1 29.183
1-30.035
1 30.859
I 30.822
MARTIN VALLEY (BUFFALO GAP) SPRINGS
(SPRINGS)
HOT SPRINGS .
CASCADE SPRINGS
'•.'','
'
- ' •.
102.994
104.598
105.342
105.311
(HOT SPRINGS)
HOT SPRINGS
"
RED BULL SPRING
INDIAN HOT SPRINGS
110.421
113.587
113.259
111.870
112.50 8
112.492
112.095
112.100
112.106
112.199
112.108
.112.554
112.857
112.909
113.201
111.855
111.644
111.693
112.805
112.727
113.428
113.408
113.394
113.993
(WARM SPRING)
VEYO HOT SPRING
' ;
DIXIE (LAVERKIN) HOT SPRINGS
REDMOND SPRINGS (LAKE)
MEADOW HOT SPRINGS
HATTON (BLACK ROCK) HOT SPRINGS
RICHFIELD WARM (HOT) SPR1N3S
RED HILL HOT SPRING
MONROE (COOPER) HOT SPRINGS
JOSEPH HOT SPRINGS
JOHNSON WARM SPRING
(WARM VAPOR) '
ROOSEVELT (MCKEANS) HOT.SPRINGS
RADIUM (DOTSONS) WARM SPRINGS
THERMO HOT SPRINGS
GOSHEN'WARM SPRINGS
LIVINGSTON WARM SPRINGS
STERLING (NINEMILE) WARM SPRING
FUMAROLE BUTTE
BAKER (ABRAHAMt CRATER) HOT SPRINGS
WILSON HOT SPRINGS
BIG SPRING (NORTH SPRINGS)
FISH S.=>RINGS
GANDY WARM SPRINGS
'
UTAH
UT
UT
UT
UT
• UT
1
1.
2
1
1
2
3
57
I
54
37
28
UT
'UT
UT . 4
• UT 5
48
49
• UT' 6
UT . 7 47
UT 8
• UT 9
51
UT 10 53
• UT 1
52
UT
1 17
UT
2 31
UT
3 35
UT 1
• UT 2
24
1 20
UT
UT 2 . 21
UT
3 22
UT 4 25
91
.93
107
71
105
100
. 73
163
147
147
77
190
96
193
70
73
72
74
138
168
82
82
82
32
36
42
22
41
37
23
76
64
64
24
37.700
.37-329
37.189
38.993
38.864
3 8.849
.,38-776
38-538
38.532
58.611
38.602
W.
38.588
88
33.496
38.211
35
90
38.173
21
39.955
22
39.246
22.
59.180
23
59,614
39,511
87
75
39.905
27
39.884
27
39.341
0 59.456
27
"•'
TEMPERATURE 5 ^
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^ ^
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2
" * ° . . .?
3
NAME OF SPRING
,;/
? f " u T .1 19A^ 86 29 1 .40.465' 109-219 SPLIT MOUNT AIN WARM SPRINGS
''
' •: j OT 1 11 . 132 55 1 40-815 111-915 BECKS HOT SPRINGS
: .UT 2 12
105 40 0 40-790 111,-895 WASATCH HOT SPRINGS
UT • 3
115 46 I 40.532 111.478 WARM DITCH SPRING
• UT 4 14
100 38 X 40.523 111-490 MIDWAY;HOT SPRINGS (SCHNEITTER S HOT POTS
,. UT 5 ' 14B 1 0 4 39 1 40.524 111.468 MIDWAY.HOT SPRINGS CBUHLER S SPRINGS) .
UT ,' 6 14A . 115 46 I 40-516 1X1.475 MIDWAY: HOT SPRINGS (LUKE S H O T POTS)
.. • U T .7 .13
136 58 0 40.487 111.911 CRYS.TAL, HOT SPR INGS .
"
UT 8
W P 40-353 111.895 CRATER HOT SPRINGS
;:. UT 9 15
111 43 .1 40.348 XXX.908 SARATOGA HOT SPRINGS
/
UT XO-;/
77,. 24 0 40-240 1 X 1 - 8 6 5 (WARM SPRINGS) ...1
*// UT 11
75 23 0 40.232 111.868 (WARM SPRINGS)
:.;;UT,,12,'
86 29 0 40.177 1 1 1 . 8 0 1 : . y ^ - ; , " 7 .•;*•
' UT 13 16
.89 31 0.40.144 111.307 LINCOLN POINT WARM SPRINGS
/ . UT. 14 19
67 20 I 40.118 111 .341 DIAMOND FORK WARM SPRINGS .
UT 15 1 8
111 44 I 40.041 111.530 CASTILLA SPRINGS .
UT i
9
..W 1 40.733 112.647 BIG WARM SPRINGS
UT 2
1^,1 40.667 112.677 BURNT .SPR INGS
. UT 3 10.. 90 32 , 1 40.644 112-523 GRANTSVILLE WARM SPRINGS
UT" 4 •
_
1 40.533 112.595 MUSKRAT SPRING
...
- UT 5
W 1 40.513 112.712 HORSESHOE SPRINGS
UT 6
U 1 40.559 li2.741 lOSEPA (DESERET) SPRINGS
UT ' 7 lOA
80 . 26 I 40.397 112.418 MORGANS WARM SPRINGS
UT 8 lOB
80 27 1 40.388 112.424 RUSSELLS WARM SPRINGS
UT .. 1
8
135 57- 0 41.232 111.929 OGDEN HOT SPRINGS
,
UT 2
77 2 4 . 1 41.035 111.658 COMO;WARM SPRINGS
/• UT 1 / 3
110 43 1.41.855 112.157 UDOY HOT SPRINGS '
UT 2
2
86 29 I 41.832 112.455 BLUE CREEK SPRING (BLUE WARM SPRINGS)
UT 3
80 26 0 41.836 112.056 CUTLER WARM SPRINGS
•UT 4
75 23 /O 41.722 112.256 BOTHWELL WARM SPRI.NGS'
UT 5
4
134 57 1 41.659 112.086 CRYSTAL (MADSENS) SPRINGS
UT 6
4A
90 32 0.41.584 112.240 LITTLE MOUNTAIN WARM SPRING
• UT 7
124 51 1 41.579 112.232 STINKING SPRINGS
UT 8
6
137 58 I 41.339 112.032 UTAH^(BEAR RIVER) HOT SPRINGS
UT 9
5
84 28 I 41.233 112.415 (SPRING).
•UT 10
139 60 1 41.138 112.169.HOOPER HOT SPRINGS
UT 1
1
80 26 1 41.755 113.602 (WARM S P R I N G )
UT 2
107 41 1 41.587 X13.985 (SPRING. (HOT))
!
:
..
.
-
•
-
•
•
.
-.
•
.
,
j
WASHINGTPN
WA 1
WA 2
WA 3
WA ,4
.•'ulA 1
•WA
1
100
' 120
16
12
89
90
69
37
49
1
1
HI
32 I
32 1
21 I
45.823
45.728
45.723
45.553
45.452
46.752
121.116
121.800
121.927
121.962
120.959
121.814
KLICKITAT SPRINGS
ST MARTINS HOT SPRINGS
GRAYS HOT SPRINGS .
MOFFETTS HOT SPRINGS
SODA SPRINGS
LONGMIRE
f
CS
TEMPERATURE 5 '
,-*
r*
-f.
;«
C9 U J
UJ
H-
;? s
«,VI
£
S
»3
3
3
NAME OF SPRING
CO
^ • WA
- WA
- WA
WA
. WA
• WA
WA.
WA
WA
, • WA
• WA
• WA
• WA
• y A
- • WA.
12.0
455
••2
3
4
5
1
1
2
3
4
1
2
1
2
3
4
1:28
14
12A
5
7
:;8
9
3
2
. 1
4
75
190
.100
1:22
127
122
125
132
107
.98
139
109
4 9 -1 46.738 121.562
13 0 46.703 121.485
H :i 46.202' 121.452
24
1 46.005 121.191
87
0 46-215 122.188
38 I 47.892 121.342
.4'9 0.47.710 121.152
32
I 47.4,84 121.391
49 I 47.201 121.536
52
1.47.977 123-682
"56 1-47.969 1 2 3 - 3 6 4
42 I 48.763 121.567
37 X 48.254. X2X.X70
60
3 48.172 X21.039
43
I 48-118 121.192
OHANAPECOSH HOT SPRINGS
SUM.MIT CREEK
(SODA)..
MOUNT ADAMS C R A T E R
(SPRINGS)—
MT ST HELENS FUMAROLE
GARLAND .MINERAL SPRINGS
SCENIC- (GREAT NORTHERN) HOT SPRINGS
GOLOMEYER HOT SPRINGS
(HOT SPRINGS)'
OLYMPIC HOT SPRINGS
SOL DUC HOT S P R I N G S :
BAKER HOT S P R I N G
SULPHUR HOT SPRINGS .
GAMMA HOT SPRING
KENNEDY HOT SPRING -
.WYOMING
WY
WY
WY
. WY
WY
. WY
WY
WY
> WY
WY
-WY
WY
WY
WY
WY
WY
WY
•WY
WY
WY
WY
UY
WY
WY
WY
WY
WY
WY
WY
1
1
1
1
1
1
2
1
1
2
3
1
2
3
1
2
1
2
3
4
5
6
7
8
9
1
2
1
•2
115
116
114
113
112
110
105
103
111
10 8
10 6
107
102
101
104
98
' 99
97
12 0
69
85
129
75
60
89
102
143
114
• 60.
13 2
71
111
84
75
121
112
80
64
80
85
112
93
85
67
69
96
48
21
30
54
24
16
32
39
62
46
16
55
22
44
29
25
50
45
27
18
27
30
45
37
30
20
21
36
41.449 106.80 2
4 2.24 9 104.779
42,663 105.395
4 2.545 105.723
4 2.7 03 107.103
42.313 108.033
42.491 103.171
42.747 109.618
4 2.,827 110.997
42.817 110.993
42.595 110.507
45.654 108.195
43.582 108.209
43.009 108.,837
43.560 109.729
45.520 109.670
4 5.953 110.593
.43.910 110.189
43.637 110.614
43.624 110.605
43.545 110.739
43.4 71 110..-835
43.367 110.44 4
43-296 110.774
43.282 110.0 20
4 4.73 5 10 3.188
44.612 108.136
44.512 109.115
44.493 109.204
SARAT OGA HOT SPRINGS
IMMIG RANTS WA SH TUB (WARM SPRINGS)
DOUGL AS WARM SPRINGS (3)
ALCOV A HOT SP RINGS
HORSE CREEK S PRINGS
CONAN T (3)
(WARM SPRINGS
STEEL E HOT SP RINGS'AUBUR N ...WARM S PRINGS
* .
JOHNS ON SPR IN GS (3)
BIG F ALL CREE K (3)
THERM O P O L I S ( BIG HORN) HOT SPRINGS
WIND RIVER CA NYON (3)
WASHA KTE MINE RAL HOT SPRINGS
WARM S P R I N G ( 3)
LITTL E ; W A R M S PRING (3)
,
JACKS ON LAK.E HOT SPRINGS. '.
NORTH BUFFALO FORK (3)
KELLY WARM SP RING
TETON VALLEY WARM SPRING
ABERC ROMS IE W ARM SPRING
BOYLE S HILL S PRING (3)
GRANI TE HOT S PRINGS AND GRANITE FALLS (3)
ASTOR IA MINER AL HOT SPRINGS
KENOA LL WARM SPRING
LITTL E SHEEP MOUNTAIN WARM SPRINGS
SHEEP MOUNTAI N WARM SPRINGS
PEMAR IS (CODY ) HOT SPRINGS
(
3UFFA LO BILL RESERVOIR (3)
•,7^-kS.-
..-/t. 'J.\-.':
ca
TEMPERATURE i
ae t >
* 12
NAME OF SPRING
WY
WY
WY
WY
.. WY
- WY -
- WY
. UY
WY
•' WY
WY
•/. WY
: WY
/ WY
• WY
WY
;.wY
WY
WY
WY
. WY
WY
• WY
WY
WY
WY
. WY
WY
WY
:W.Y
WY
WY
' -WY
WY
WY
WY
WY
,WY
WY
WY
WY
. WY
..•WY
WY
WY
- WY
WY
WY
'
1
2
3
4
5.
6
7
8
9
10
11
12
13
14
15
•15.
17
18
19
20
21
22
25
24
25
26
27
28
29
30
31
32
33
34
35
36
37
38
39
40
41
42
43
44
45
46
47
4«
1
•
2
55 A
56
.3
57
7
:7A
.8
136,
165
15 5
195
198
156
58
50
73
9
•69
52
9A
75
198
13 4
195
72
75
76
11
78
11
55
54
77
79
12
13
14
81
15
16
16A
33
201
197
197
180
56
51
194
19 3
195
183
190
198
199
87
51B
57
59
92
193
4 4 . 9 81
44.967
44.906
H
44.841
H
44.825
H I 44.825
1 4 4.796
91
X 4 4^787
92
1 4 4.779
68
H I 44.779
H 1 44.771
H. 1 4 4 . 7 6 7
92
1 4 4-. 7 62
1 44.757
84
I 44,757
;H I 4 4 , 7 5 1
H I 44,750
H- 1 4 4 . 7 4 9
1 44-746
91
I 44.740
I
44.740
92
H 1 44.741
H I 4 4.733
91
I 44.725
H 1 44.721
87
44.716
H I -4 4 . 7 1 4
H I 44.712
•H 1 . - 4 4 . 7 02
H 1 44.596
87
1 4 4 . 5 96
92
1 44.695
92
I 44.589
» 1 44.587
H
94
1 44.685
•91
1 44.583
91
1 44,575
B2
1 44.673
H 1 44.673
H I 44.556
89
I 44.648
1 44.634
90
1 44.522
H 1 44.615
44.604
H
44.598
H
44.598
H
44.598
H
58
74
58
110 . 68 3 HOT RIVER
110.708 MAMMOTH HOT SPRIN.SS
110.395 CALCITE SPRINGS.
110.16 7 (HOT- SPRINGS)
110-673 tSAS VENTS)
110-114 WAHB SPRINGS
110-725. AMPHITHEATER ;SPRIN3S
110-735 CLEARWATER -SPRINGS AND SEMI-CENTENNIAL GE
110-697 WHITEROCK SPRINGS
110-737 (STEAM VENTS)
110-25 5 RAINBOW HOT SPRINGS
110.305 (HOT'SPRINGS) ^
110.450 WASHBURN , HOT SPRINGS AND SULPHUR CREEK H
110-305 COFFEE POT HOT SPRINGS
110-733 BIJAH SPRING . . . .
110-254 (HOT. SPRING)
110 - 4 0 9 (HOT SPRINGS)
110w7l2 FRYING PAN SPRING AND (GAS VENT)
11 0 - 22 5 HOT SPRING BASIN GROUP
110,-699 ( G A S V E N T S )
110-329 WHISTLER GEYSER AND JOSEPHS COAT SPRINGS
110.256 HOT SPRINGS BASIN GROUP
110.035 ..(HOT. SPRINGS)
110.70 5 NORRIS GEYSER BASIN
110.355 (HOT SPRINGS)
110.702 ECHI.NUS GEYSER (NORRIS GEYSER BASIN)
110-557 (GAS -VENTS) . •
110.475 FOREST SPRINGS
• .
.
110-034 (HOT SPRINGS)
^
110-378 (HOT SPRINGS)
110.758 SYLVAN SPRINGS
110.722 GIBBON HILL GEYSER
110.75.3 ARTISTS .'AINTPOTS
110.327 (HOT SPRINGS)
110-727 GEYSER SPRINGS GROUP.
110-753 MONUMENT GEYSER BASIN
110-750 BERYL SPRING
110.295 PONUNTPA SPRINGS GROUP
110.237 (HOT. SPRINGS)
110.570 VIOLET SPRINGS
110.489 SULPHUR SPRINGS
110.231 THE MUDKETTLES AND THE MUSHPOTS
110.436 SULPHUR CAULDRON, MUD VOLCANO, AND OTHERS
110-617 HIGHLAND HOT SPRINGS
110-617 (HOT SPRINGS)
110-630 (GAS. VENT)
110-235 (HOT. SPRINGS)
110-211 PELICAN SPRINGS
I •
.'
.Ih-iitr.fl-..
TEMPERATURE = i
rUJ
O H—
_JE
« UJ
?
^
VI C O
r •WY 49
WY 50
•WY 51
WY 52
WY 53
'WY 54
WY 55
WY 55
.WY 57
WY 58
WY 59
WY 60
,WY 61
WY 62
WY 63
WY 64
'WY '65
WY 66
WY 67
WY 68
• WY 69
WY 70
WY 71
WY 72
WY 73
WY 74
WY 75
WY 76
WY 77
WY 78
. WY 79
WY 30
. WY 81^
WY 82
WY 83
WY 84
WY 85
WY 86
WY 87
WY 88
WY 89
WY 90
WY 91
WY 92
WY 93
WY 94
WY 95
WY 9-6
NAME OF SPRING
89
196
,,.—..
91
H
,H
H
204 95
H
H
20 3 94
18
160 71
17
H
202 95
93
H
93
21 • 199
94 , 197 92
202 94
2 0;
201 9 4
204
95
22
198 •92
.95
202 94
2"4
199 93
25
201
93
26A
190
87
96
202
95
29
192 89
205 96
30A
.34 . 199 92
200 93
35A
158 69
35
90
91
.19
27
63
200 . 93
35
37
64
20 0
93
36
38
42
44 A
202
199
201
95
93
94
195
154
91
67
141
61
40
39
41
45
43
48
47
H
P
- - ,
44.594 110.319 (HOT SPRINGS)
•
.••'"••••
•.4 4.59 2 110.61 9 (GAS VENTS)
; / • / , - • ', ^ _' '':"'•
.4 4.587 110.^332 EBRD-SPRINGS • -'
'
• •./''
-•4 4 . 5 8 2 110.312 V E R M I L L I O N SPRINGS " ;
,44.571 1 1 0 . 8 0 5 HORNING Ml'ST SPRINGS AND QUAGHIRE GROUP !
.... . . „ : , . .'
..-'..
.44.570. 110-691 (HOT,:SPRI.NGS)
," ,
Z ' - •/.
4 4 . 5 6 8 1 1 0 . 8 5 1 FLAT CONE SPRING R
I
V
E
R
:
G
R
O
U
P
SPRINGS
'
'
"
.
•
:
/
4 4.565 1 1 0 . 8 3 1
44.563 11Q.871
/
4 4 . 5 5 7 1 1 0 . 8 4 7 RED T E R R A C E SPRING A N O . Q U E E N S L A U N D R Y
'4 4.555 1 1 0 . 8 1 3
•...,,"
' •: "
::44-5.54 :110-301 FOUNTAIN GROUP
.BEACHHOT
SPRINGS
'
.
:
.
.
"
=
,
,^
..
:
:
:
':
:
/
.44-547 110-807
":.••.../•/
44-545: 110-25 7 FOUNTAIN PAINT POT ' ' " V. .
" / - ' "/'
44-543 110-859 TURBID SPRINGS .. .:-",-"''':::
:
•:/••-:,:
44-543. lib-790 F A I R Y " S P R I N G S . : . - ; ' ' :
44,534 110-798 HOT LAKE .ANDFIREHOLE LAKE
44-529 110-296 WHITE OOME GEYSER-AND GREAT FOUNTAIN GEY44.529 110-878 STEAMBOAT SPRINGS
44.523 110-837 IMPERIAL GEYSER AND SPRAY GEYSER
44.520 110-814 EXCELSIOR GEYSER CRATER AND GRAND PRISMA!
44.519 110-27 5 (HOT SPRINGS) (RABBIT CREEK AREA)
; .
44,483 .110*854 BUTTE SPRINGS .
44,473 110-863 SAPPHIRE POOL AND OTHERS
," •
44,4 72. 110-844 HILLSIDE SPRINGS
OT
MORNING
GLORY
P
O
O
L
,
G
R
O
T
T
O
GEYSER,
AND
44.458. 110-825
44.4 61 110-839 OLD FAITHFUL GEYSER AND OTHERS
44.458 110-852 :CASTLE GEYSER (BLACK SANO BASIN)
4 4.43 6 110-974 EMERALD PO=OL AND.OTHERS'
.-*...
44.432 110-578 (HOT SPRINGS)
POTTS
HOT
SPRING
BASIN
44.432 110-809
44.423 110-95 2 (HOT SPRINGS) '
4 4.418 110-802 •SMOKE JUMPER HOT SPRINGS .;
.
44-415 110-569 LONE. STAR GEYSER
WEST
THUMB
GEYSER
BASIN
44-407 110-821
44-403 110-937 (HOT SPRINGS)
44.551 110-795 (HOT SPRINGS)
44.515 110-655 SHOSHONE GEYSER BASIN
44.505 110-530 (HOT ;SPRINGS) .
44,289 110-504 (HOT SPRINGS)
44.291 110-883 (HOT SPRINGS)
44.282 110-899 THREE RIVER JUNCTION SPRINGS
44.2-83 110-879 BECHLER. RIVER HOT SPRINGS
44.279 110-505 TENDOY FALLS SPRINGS
44.274 110-640 RUSTIC GEYSER
44,203 110-485 (HOT SPRINGS)
44.180 110-72 7 (HOT SPRINGS)
44.165 110-583 (HOT SPRINGS)
SNAKE RIVER (SNAKE) HOT SPRINGS ( 5 ) '
"• : ) ^ T
'
•-
.
>•'
. .v.
-
.
.
»
- ^ • • .
IL
TEMPERATURE = :
CO
CO
V>
ac.^
S
•«
-3
CO
NAME OF SPRING
•f-
WY 97
WY 98
46
• WY 9 9 100
. WY
1
159
H 1 44-155
B 1 44-141
71 1 4 4 . 1 1 3
H I . 44.245
v.-"C-
110.698
110-656
110.684
111.022
(HOT SPRINGS)
SOUTH ENTRANCE HOT SPRINGS (.5) "
HUCKLEBERRY, (FLA6G RANCH) HOT SPRINGS (5
(HOT SPRINGS) ,.
- **
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September 21, 1979
MEMORANDUM
TO:
ESL Staff
FROM:
Mike Wright
SUBJECT:
Management of the Geochemical Laboratory and Staff
As you all know. Bob Bamford plans to leave ESL in order to pursue
private consulting. Therefore, effective 1 October 1979, Joe Moore will
assume responsibility for management of the Geochemical Laboratory facility
and staff. Reporting directly to Joe will be the current lab staff, including
Odin Christensen, Regina Capuano, Dave Cole, Ruth Kroneman, and Tina Serling.
Joe will be responsible for implementing new programs planned for FY80,
for continuation of the current programs, for ensuring the quality of the
analytical and other work produced by the lab and for assigning priorities.
Requests for lab staff assistance and for analytical work should be
communicated to Joe.
After 1 October, Bob will be working as a consultant to ESL. He will be
working at the lab full time until about the middle of October, when the
initial writing for the Roosevelt Hot Springs report will be completed. At
that time, Dave Cole will be taking over Bob's office space, and Bob's work
for ESL will be on an as needed basis until The Geysers work is complete.
Odin Christensen will assume primary responsibility for the Roosevelt and
Geysers studies on behalf of ESL after 1 October and will interface with Bob
on Bob's continuing contribution.
We have very much appreciated the excellent work which Bob has directed
while at ESL. Industry has recognized this work as being highly interesting
and significant. Those of you who have contributed to the success of the
geochemical research efforts to date can be justly proud.
Mik"e Wright
Associate Director
MW:srm
ANACOMPA A
From
DENNIS LNIELSON
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SUBREGION DESCRIPTIONS
SUBREGION I:
'Xi^-^y.eJi txbt..
SNAKE RIVER PLAIN
Subregional Setting
The Snake River Plain and the Yellowstone volcanic field
constitute a major young volcanic province extendi-ng in a broad
arc from the Idaho-Oregon sta-te linq eastward across Idaho tc
/
Yellowstone National Park and vicinity (Figure 1).
The common
geologic element in the region is the volcanic activity as
indicated by the young basaltic rocks at Craters of the Moon in
the eastern Snake River Plain and the massive young rhyolitic
volcanic deposits and associated basalts of the eastern Snake
River Plain and Yellowstone.
The Snake River Plain is an area of generally low relief which
is covered by basaltic lava flows interbedded with young, flatlying river and lake deposited sedimentary rocks.
The plain
contains a large proportion of the state of Idaho's irrigated
agricultural lands, and most^of its population centers.
The northeastern portion of the plain is terminated by a generally
circular, forested, silicic volcanic feature, the island Park
Caldera.
The island Park Caldera borders the higher plateaus
and mountains of Yellowstone National Park immediately to tha
east.
Radiometric dating indicates that the volcanism has pro-
gressed eastward along the plain toward Yellowstone.
r -;>
The Eastern plain has been characterized as a downwarp, and
geophysical surveys indicate 3 to 5 Kws of sedimentary and
volcanic fill within the trough.
The primary recharge area for
the Snake Plains Aquifer is the high snowfall region in the
island park area.
The outflow area is at Thousand Springs near
Buhl in the canyon of the Snake River.
Scattered young silicic
volcanic centers are present both within the Eastern plain and
marginal to it within the Blackfoot Volcanic Field.
The Western plain has been described as a rift valley.
Volcanism
in the Western plain is older than that of the Eastern plain and
no specific prospects based on young rhyolitic volcanism have
been identified.
Economy of the Subregion
The agricultural emphasis in both the eastern and western Snake
River Plain is on potatos and sugar beets.
Associated food pro-
cessing industries are a maqor agribusiness element of the subregion.
Alfalfa and grain are also of agricultural significance in the
subregion.
The Island Park area supports an active timber industry.
The most significant mineral industry in the region is also
agriculture-related.
Extensive phosphate deposits occur in the
region marginal tp the Snake River Plain in southeastern Idaho
and significant phosphate processing industry is centered at
Pocatello.
\ •»
-i
Energy Production and Consumption
At present, wnergy generation within the subregion is dominantly
hydroelectric, with extensive generation capacity developed by
the Idaho Power Company from reservoirs along the Shake River,
and imported electric power from the Columbia River system provided by the Bonneville Power Administration.
Idaho Power
Company and rural electric coops are seriously considering
alternative electrical generation alternatives as the hydroelectric
generating capacity of the Snake River system has been developed
to near-capScity.
Coal-fired plants have been proposed to meet
projected requirements but specific projects have been rejected
on environmental grounds.
The major supplier of energy for direct heat uses in the subregion is the Intermountain Gas Company.
The company is agressively
investigating geothermal markets, ma»y of which (as at Boise)
have tPQ-dit'ionally used geothermal energy for direct, heat
applications.
Geothermal Potential
Confirmed geothermal resources of the area are of low and moderate
temperature/ and are presently being exploited for a variety of
direct heat -uses.
Known geothermal resources within the sub-
province are primarily associated with normal faulting along the
margins of the Snake River plain.
4.
Young silicic volcanic rock within the Eastern plain and the
high temperature geothermal systems at Yellowstone National Park
indicate the potential for igneous-related high temperature
resources in the Eastern plain.
The high flow rate Snake Plains
Aquifer is responsible for obscuring the high heat flow that may
be associated with such hidden resources.
Moderate temperature hydrothermal systems are indicated by geochemical thermometry for the Western Snake River plain.
High
temperatures (-200°C) have been reported from deep exploration
wells in the area, but no high temperature fluid production has
been confirmed.
The fracture zones paralleling the northv/estern trend of the
plain contain at least moderate temperature geothermal resources
along both the northern and southern flanks of the Western Snake
River plain.
The Bruneau-Grandview area adjacent to the plain
on the south is notable in this respect.
At least a 12 by 60 mile
atea contains hot fluids at depths of 1,000 to 3,000 feet. Thie
region may ext end from Twin Falls near the easternmost portion
of the Western plain more or less continuously to the Oregon state
line near Vale.
Strategy
Based on existing resource data, near-term geothermal utilization
within the subr egion will be primarily a continuation and
expansion of direct heat applications of the low and moderate
temperature hydrothermal resources.
The Technical Initiatives
Program (TIP) insures that potential users are made more fully
aware of the geothermal potential existing throughout the subregion and, together with the PON program for direct heat
application, will maximize the replacement of fossil fuel used
to..create low grade energy with geothermal resources. • The
Midterm electrical generation goal of 8,000-9,500 M\7e from high
temperature Esources will be largely dependent on the successful
exploration for the hidden resources of the deep Snake River
plain.
Impediments to industry exploration cf the subregion
without government support include both the masking of the deep
thermal situation by the cold Snake Plains Aquifer and the
drilling difficulties anticipated in drilling ' through the
volcanic sequence.
A combination of ongoing USGS and DOE-supported
assessment, combined with cost-shared drilling with industry,
is expected to establish the high temperature geothermal
potential of.the Snake River plain by 1982.
The midterm utilization of the extensive moderate temperature
•resources for electrical power generation will depend on the
successful development of moderate temperature electrical
generation technology at Raft River.
^-.;
SUBREGION II - NORTHERN ROCKY MOUNTAINS
Subregional Setting
The Northern Rocky Mountain Subregion (Figure 1) is a mountainous
area characterized by rugged topography, extensive forests and
low population density.
The subregion is here defined as those
portions of Montana and Northern Idaho characterized by the
presence of batholiths and folded mountain ranges exclusive of.
the young volcanic provinces of the Yellowstone and Snake River
plain.
The combined Idaho and Boulder Batholiths comprise much of .
central Idaho and southwestern Montana.
The area geologically
is dominated by batholithic complexes of intermediate to silicic
rocks of Cretaceous age (90MYBP).
The batholiths are similar in
composition and age to the Sierra Nevada Batholith.
The southern and western margins of the Idaho Batholith contain
faulted sedimentj:basins such as Little Camas Prairie, which
provide ideal reservoir conditions with approximately 2 KM of
sedimentary fill.
In addition to the batholithic ranges', the subregion contains
north-trending, folded, sedimentary mountains such as the Sawtooth
Range in central Idaho.
oJ
Economic Parameters
As the subregion is dominantly dorested land, the econoitiy is
based on forext products, tourism, agriculture and hard-rock
mining.
Population density is low and much of the subregion
is composed of National forests, wilderness areas and primative
areas.
Energy Production and Consumpsion
Electrical generation within the subregion is a mix of hydroelectric power imported from the BPA and Snake River systems,
coal fired generation at the Jim Bridger Plant near Green River,.
Wyoming, and smaller local hydro and coal fired plants.
Domestic and Canadian natural gas provides the most important
energy source for direct heat applications throughout the subregion.
Concern over natural ga-s availability has motivated
widespread interest in alternative energy sources for direct
heat applications.
Geothermal Potential
The Northern Rocky Mountain Subregion has a widespread potential
for the discovery and development of moderate and low temperature
geotheraal resources.
There is no geochemical or geologic
evidence for the existence of very high temperatures suitable for
electrical power generation.
Widespread moderate and low
temperature resources are localized by the presence of fractures
• ' /
and fault zones.
Heat flow throughout at least the Idaho
Batholith and Boulder Batholith is known to be high and virtually
any recently active fault zone within this portion of the subregion has a potential for providing a moderate temperature
resource through deep convective circulation.
Hot springs and
shallow, moderate temperature, hydrothermal resources are particularly common along structural zones within the Idaho
Batholith.
Strategy
The geothermal program in this subregion will emphasize the
stimulation of the development of moderate temperature resources
for direct heat applications.
Individual communities and
industries within this natural gas-dependent area will provide
the primary targets for development of the geothermal resources
for direct heat applications.
The program will be implemented
largely through the TIPS project and a continuation and expansion
bf the PON program.
The wide-spread occurence of hard rock
mining throughout the subregion presents both an opportunity
for expanded utilization of natural hot waters in mineral beneficiation and an institutional question concerning the status
of geothermal rights versus mineral rights.
9.
SUBREGION III - WASATCH FRONT
Subregional Setting
I*'
"
. The Wasatch Fault Zone and -its_northern-continuation-as-the
^;
•
—
- > ' . , ,
^
'
..
I
Teton Fault Zone \ through southeastern Idaho .'^Hio the southern
border of Yellowstone volcanic field, .contains a disproportionate
\percentage of> the,subregion's population-and.land suitable for
agricultural purposes.
The K^arsatch-JFault-Zone.-marks a sharp
.'
boundary between the Basin.and Range Province to the west and
I
the Wasatch Range to -the east.
I -
Wasatch Front Subregion
The western margin of the
generally corresponds to a zone of
seismic activity known as the Intermountain Seismic Belt, which
continues on northward in the Northern Rocky Mountains past
I
Yellowstone through western Montana^ to the Canadian border
near Glacier National Park.
The Unita uplif^t, the Wind River
Range and the associated overtHrust belts are also included
within.this subregion.
Economy of the Subregion
The.Wasatch Front Subregion is generally lightly populated
forest land with forest products and ranching dominating its
rural economy.
A narrow strip along the western margin of the
subregion, the Wasatch and Teton Fault Zones, contains most of
the area's major population and trade centers including Salt
^
•
-•/
10.
Lake City.,, a major intermountain commerce and tranfeportationcenter-
This same area also includes much of the subregion's
crop land.
The subregion contains the watershed for several
major drainages, but the populated portions of the area remain
relatively water short.
Water constitutes one of the major
restrictions on the economic growth in the subregion.
Energy Production and Consumption
The subregion is a net importer of energy.
Both coal and
petroleum are imported from the Colorado Plateau immediately to
the east of the subregion in the state of Utah.
Utah Power and
Light, the principal electrical utility for the southern half
of the region currently purchases power from BPA and has tentatively contracted with Phillip
for geothermal steam from the
t
Roosevelt field, in south central Utah.
Geothermal Po tsntial
The techonically active margins of the subregion, which border
the Basin and Range Subregion, contain low and moderate temperature geothermal resources suitable for direct heat applications.
The general absence of young volcanism within the subprovin.ee
is negative evidence concerning the potential for the discovery
of the +200°C fluid resources suitable for electrical generation
in the near term.
The fortunate coincidence of the area's
population centers with widespread low to moderate temperature
resources associated with the Wasatch Fault Zone provides a major
opportunity for direct heat applications.
.7
11.
Oil and gas exploration of t}ie overthrust belt of southeastern
Idaho has provided Tirect confirmation of the presence of
moderate temperature resources.
Water near the boiling point
has been produced from carbonate aquifers at depths of less than
2 km at several points in Teton Valley.
Strategy
^
The near term geothermal program for the Wasatch Front subregion
f
will emphasize the acceleration of the development of low and
moderate temperature resources for direct heat applications.
This will be accomplished by means of the inventory of these
resources in cooperation with state agencies in Utah and Idaho
and the geothermal program of the U. S. Geological Survey.
Following the initial inventory of the resources which will be
completed in FY 78, the program will emphasize site specific
studies and projects under the TIPS Project designed to bring
the resource to the attention of the'potential users.
A sig-
nificant impact on new energy requirements for low grade heat
will be possible through an ambitious program which addresses
markets in the private and public sector.
•' /
12.
SUBREGION IV - COLORADO PLATEAU
Subregional Setting
The.Colorado Plateau and the young volcanic ranges which occur
around its margin with the Basin and Rande Province are here
considered as a single subregion.
The Colorado Plateau is
roughly a circular area bounded on the west and south by the
Basin and Range Province and on the north and east by the
Wasatch Front and southern Rocky Mountains.
Topographically,
the plateau is divided into a number of individual uplifts and
basins which range in elevation from 5,000 to 11,000 feet.
The margins of the plateau contain a number of relatively young
volcanic ranges with a significant geothermal potential.
These include the Mineral Range in southwestern Utah, the San
Francisco Peaks near Flagstaff, Arizona, the White Mountains in
southcentral Arizona, the Zuni Uplift in northwes-tern New
Mexico and the San Juan Range of Southwestern Colorado.
Economy of the Subregion
The subregion contains an abundance of mineral resources,
including coal, oil and gas, uranivim, and precious metals.
The area is, in general, sparcely populated with scattered
commerce centers, such as Flagstaff, serving large geographic
areas.
A number of cities have prospered in the Four Corners
region as a result of oil and gas production and uranium
•7 •'
13
exploration and development.
Coal mining is a major activity
within the Uinta region and the Kaiparowits Plateau field.
Agri-
culture in the form of truck farming and orchards is an important
local source of income in the-valleys marginal to the plateau.
Much of the land is semi-arid and supports sheep and cattle
ranching.
Energy Production and Consumption
The subregion is a net exporter of energy as a result of the coal
generation plant at Four Corners.
The oil and gas fields of the
subregion include the Uinta Basin, and the numerous fields in the
Paradox Basin and the San Juan Basin.
Energy consumption within
the region is low, but the region presents major opportunities for
the growth of energy-intensive industries co-located with the coal
deposits and geothermal resources.
Geothermal Potential
The interior of the Colorado Plateau is generally thought to be a
relatively low heat flow province.
The margins of the plateau,
however, contain major, confirmed, high-temperature geothermal
systems associated with young silicic volcanic centers.
The
Roosevelt-Cove Fort-Sulfurdale-Thermo KGRAs in southcentral Utah
constitute a major electrical generation resource which is
being actively developed by industry with DOE support.
'/
14
Young volcanic centers in central and eastern Arizona include the
San Francisco Peaks and the White Mountains.
These regions have
not been explored by deep drilling but appear promising on the
basis of their geologic setting, regional heat flow measurements
and limited geochemical data.
The Zuni Uplift in northeastern
New Mexico is interesting but its potential is less substantiated.
Strategy
The young volcanic fields marginal to the Colorado Plateau constitute a high priority target within the total region.
Accelera-
tion of the rate of development of the known fields in southern •
Utah in order to meet the 1985 goal of 100 MWe and the year
2000 goal of 2600 MWe will be accomplished primarily by means of
the industry-coupled drilling' program which was initiated in
FY 77. Further drilling in adjacent KGRAs will be encouraged
during subsequent solicitation programs.
The rate of development
of these reservoirs will also be accelerated by means of case
studies of the data set provided by the industrial participants in
the program.
The utilization of by-product fluids produced by electrical generation at these fields will be encouraged through an expanded regionwide PON program for direct heat applications.
y
15,
Oil and gas exploration within the Colorado Plateau will be carefully monitored for abnormal gradients encountered during the
oil and gas exploration.
The margins of the plateau will receive
particular emphasis in state-USGS cooperative origrans with
Arizona, Utah, New Mexico and Colorado.
These programs are
designed to target reservoirs suitable for direct heat applications,
which the TIPS Project will help make available to potential users.
•- y
16,
SUBREGION V - BASIN AND RANGE
Subregional Setting
The Basin and Range subregion is a major physiographic province
which includes most of Nevada, southwestern Arizona, western Utah,
southwestern New Mexico and a small portion of southern Idaho.
The subregion includes block-faulted basins and granges which are
generally north-south trending* tnr;erugl«>ut/l^ie>jr'^g^raT\
The sub-
region is arid to semiarid and characteristically is composed of
desert lands and closed drainages.
Although basaltic and rhyolicic
lavas dated 6 to 20 million years before present are common
throughout the province, there are very few young rhyolitic centers.
The region has a higher than normal heat flow, and hot springs
and wells, particularly in northcentral and eastern Nevada.>
Economics of the Subregion
Mining and ranching provide the major regional source of income.
Tourism, forestry and agriculture are locally important.
The
availability of water throughout the region is restricted and
water requirements for any new industrial or population growth
must be carefully considered.
y
17.
Energy Production and Consumption
Due to the low population density, the Subregion is not a large
consumer of energy.
The minerals industry, however, does require
large quantities of energy for mineral beneficiation at the
numerous smelters dispersed throughout the province.
The region could be a major supplier of electrical power to
California.
Geothermal Potential
The subregion has a widespread moderate temperature resource
which is almost universally present along fracture zenes within
the region.
Geochemically predicted base reservoir temperatures
of 150° to 200°C are relatively common and temperatures as high
as 240°C are predicted for some fields.
Although the Basin and
and Range Province is characterized by its high heat flow, the
thermal gradients measured throughout the region are by no means
uniform.
High gradients are especially common in a region of
northcentral andptqrtlxea^^je&sn Nevada known as the Battle Mountain
High.
This area of unusually high heat flow does not appear to
be associated with any known igneous heat source, but rather is
an area of abnormally high gradient superimposed on the regional
high.
The area of the Battle Mountain High continues to be the object
of considerable industry interest in exploration for electrical
• •/
18,
generating capacity.
The westernmost portion and its boundary with
the Sierran Front seems to possess the high temperature geothermal
potential.
Prospects with confirmed high temperatures include
Steamboat Springs, Brady Hot Springs and Grey's Peak.
Strategy
In view of the interest displayed by industry in the electrical
generating capacity of resources of the northern Basin and Range,
this region has been targeted for the second initiative of the
industry coupled program, beginning in 1978.
Significant questions
remain as to the nature of the heat source driving the numerous
moderate and possibly high temperature systems.
The industry
coupled program will be designed to both stimulate the drilling
and development of the numerous systems in the area and also to
acquire detailed subsurface data which will be valuable in
accelerating the industries rate of successful discoveries.
\* -
y
A modest program of 10 W and moderate temperature reservoir
identification is planned in cooperation with the USGS and State
agencies.
This program will seek as its main thrust to replace
existing energy consumption in.the region for mineral beneficiation
at sites where mineral processing and the geothermal resources
are co-located.
.V
19.
SUBREGION VI
RIO GRANDE RIFT - SOUTHERN ROCKY MOUNTAINS SUBREGION
The major feature of this subregion is the Rio Grande Rift, a
structural depression located jiist west of the Sangre De Cristo
Range of Northern New Mexico, which estends southward through
Central New Mexico to the Texas border at El Paso.
Also inclu'ded
/
/
in the Subregion are the Southern Rocky Mountains, which extend
••
•
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•
-
/
/
.
•
from the Laris^mie Range in Southern Wyoming ito the Sangre De yCristo
Range.
The region is mountainous with elevations to 14,000' feiet.
)araii
The Subregion is bounded on the east by /the Great Plains yand on
the west by the Colorado Plateau and Wyoming Basin (Figure 7).
• ''
/
Economics of the Subregion
/
/
The economy of the subregion has a strong agriculture and forest
/
'
. /
products base. Tourism- has become art increasingly important
industry and environmental sensitivities are especially high.
/
/
Ranching, forestry and only a limited additional agricultural
activity is permitted by the topography and climate of the riegion.
Energy Production and Consumption
T^e area generally lacks energy intensive industries and is
neither a major producer or consumer of electricity.
Electrical
power generation from high temperature geothermal resources could
serve the needs of growing metropolitan areas/such as Albuquerque,
or could be exported to California.
Many of/the individual cities
I / >'•>
20.
and town within the subregion are dependent on natural gas for
direct heat applications and their service has been threatened
during past winters by natural gas shortages.
These urban areas
constitute the major new term market for geothermal energy
within the region.
•
/
'
Geothermal Potential
/
The subregion has a demonstrated high temperature reservoir wh»ich
is being developed by pnion Oil Company a^t theValles Caldera/near
Los Alamos in northern New Mexico.
The Caldera lies along the
Rio Grande Rift on the margin of the Colorado Plateau.
/
The/pre-
.
./
sence of high temperature geothermal reservoirs at other sites
along the Rift have been postulated but not confirmed. The Rift
/
does constitute a favorable region for high temperature geothermal
/
system discoveries.
/
•
The remainder of the subprovince, particularly
/
/
the more northern ranges, do not appea^r to have a high/temperature
potential. Known geothermal occurences through the San Luis
Valley in southern Colorado and near Alenwood Springs in northern
Colorado confirm that at least a mo.'cJerate temperature resource
is present throughout this negion./
.y- <i.
21
Strategy
A pre-commercial study of the high temperature potential of the
Rio Grande Rift will be conducted during 1979 and 1980.
Based on
the success of this survey, an industry-coupled program will be
i
initiated in 1981 which will be designed to stimulate industry
exploration for high temperature systems within the Rio Grande
Rift.
The State Coop program and the PON program for direct
i
heat applications will be employed in order to stimulate the
development of low and moderate temperature geothermal resources'
in the major population centers of the region, i
>
/ . '
22
SUBREGION VII
I
GREAT PLAINS
Subregional Setting
The Great Plains subregion is a major physiographic province
lying east of the Rocky Mountains.
For the purposes of this pro-
gram the Wyoming Basin is included within the Great Plains subregion.
The Great Plains are underlain by eastward dipping sediI
mentary rocks of tertiary age.
A number of individual mountain
ranges, including the Black Hills of South Dakot^, are present
within the subregion.
The Williston Basin is a large sedimentary
basin centered to the northeast of the Black Hills in Montana,
North Dakota and Northwestern South Dakota.
The principal deep fresh water aquifer throughout much of the
subregion is the Madison Limestone.
Economy of the Subregion
The economy of the area is dominantly agricultural, with most of
the subregion being utilized for grain production and ranching.
Oil production from the Williston Basin in North Dakota, the
Powder River, Big Horn and Wind River Basins in JWyoming, and gas
i
and oil production from several fields in Montana have constituted
I
I
major non-agriculture economic activity of the subregion.
Montana
and Wyoming contain significant bituminous to subbituminous coal
fields which are undergoing accelerated development and will
i
significantly impact the region's economy. Coal processing will
compete with other demands for ground and surface water in the
i
Subregion.
t.
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23
Energy Production and Consumption
The region is a net exporter of energy and fuel as a result of
i
its low population density and abundant energy resources.
In
i
view of the region's abundant coal deposits, coal:generation of
electricity may be water-limited rather than resource-limited.
Geothermal Potential
The Great Plains subregion contains no identified igneous point
sources and the geologic environment does not suggest the presence
of high temperature geothermal systems.
Heat flow throughout
most of the region is normal or near-normal and, as a result,
moderate temperature convective systems are not common.
The subregion does contain widespread occurrences of hot water
I
in the Madison Aquifer, which has been locally utilized for
direct heat applications.
A significant development for space
heating is presently underway in South Dakota under the PON program.
Water near the boiling point is produced from the Madison
Formation near Casper and Sheridan, Wyoming, making these urban
areas potential users of geothermal energy for direct heat
applications.
.- ^'4
•'^k. • ' •
.1
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4
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(/)<
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LxJ S -M
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I—
F O U R T H
A N N U A L
FIELD
C O N F E R E N C E
-
1 9 5 3
CHARACTERISTICS OF THE JURASSIC TWIN CREEK LIMESTONE
IN IDAHO, WYOMING, AND UTAH' UHdfEBSlTV OF UTOH
^
By RALPH W . IMLAY.
United States Geological Survey, 'Washington, D. C.
INTRODUCTION
This paper includes a summary of the lithologic
:nd stratigraphic characteristics of the seven members
if the Twin Creek limestone, the descriptions of some
ypical seaions in western 'Wyoming and southeastern
daho, and three lines of columnar sections. The last
wo items present much information not published preiously. The summary descriptions represent a conensed version of those published in the Wyoming Geo3gical Association Guidebook for 1950 (Imlay, 1950a)
ut include some additional information. Only brief
lention is made of the correlation of the members of
le Twin Creek limestone, as that subject has been disiissed fully in the Bulletin of the Geological Society of
jnerica (Imlay, 1952a). Likewise, the origin of the
arious kinds of sediments comprising the Twin Creek
mestone has been discussed amply in a report pubshed by the National Research Council (Imlay,
?50b).
)lSTRIBUTION A N D GENERAL FEATURES
The Twin Creek limestone occurs in an area of exnsive thrust faulting along the Idaho-Wyoming bor:r and in north-central Utah, extending from the
uthern end of the Teton Mountains west of Jackson,
'^yo., southward to the south end of the central Watch Range near Thistle, Utah. It also occurs east of
e area of thrust faulting in the western part of the
nta Mountains as far east as Lake Fork (Thomas and
•uger, 1946', p. 1275-1277). Widiin the area of
rusting, it thickens westward from about 800 feet to
?00 feet. The thickest measured section is at Thomas
rk Canyon, about 22 miles north-northwest of Cokele, Wyo., but the section on Stump Creek, Idaho,
3ut 8 miles northwest of Auburn, Wyo., is nearly as
ck. The Twin Creek consists mainly of medium- to
ht-gray limestone, of which most is shaly and
athers into long splinters. However, the formation
0 contains two persistent red members in its lower
rd, one cliff-forming limestone member at the top
its lower third, and one sandy member at its top.
DESCRIPTIONS OF THE MEMBERS
Member A at the base of the Twin Creek limestone
:kens westward in an irregular manner from an aver'ublication authorized by the-Director, U. S. Geological Survey. ,
age of 75 feet in western Wyoming to about 400 feet
in the Blackfoot Mountains in Idaho. Its thickness may
vary markedly within distances of less than a mile. It
is absent in the Uinta Mountains and locally absent
in the Wasatch Range of Utah.
The member is characterized by soft, brownish-red
siltstone that contains interbeds, or units, of brecciated
or honeycombed limestone. In western' Wyoming and
locally in eastern Idaho the lower part of the member
contains a conspicuous unit of brecciated gray to yellow
limestone that ranges from 10 to 50 feet in thickness.
This unit is a jumble of sharply angular blocks, generally
includes a little red siltstone, and shows faint stratification. The position of this brecciated limestone unit is
occupied by thick masses of gypsum in the southeast
corner of the Jackson Quadrangle in the EVi sec. 36,
T 36 N., R. 115 W. Locally, gypsum has been found
in the lower part of the member near the head of Crow
Creek, Caribou County, Idaho, in sec. 10, T i l S., R.
45 E. (Mansfield, 1927, p. 96). In many sections the
middle and upper parts of the member contain one or
more beds or thin units of yellow honeycombed or brecciated limestone that are generally inconspicuous. In
southeastern Idaho the middle part of the member contains a unit of dense limestone that is siliceous and bears
nodules and lenses of brownish-gray chert. This unit is
about 70 feet thick on Stump Creek in the SV^ sees. 27
and 28, T. 6 S., R. 45 E., Caribou County, and at least
140 feet thick on Williams Creek in the SE14 sec. 12, T.
2 S., R. 39 E., Bingham County. A similar chert-bearing
limestone generally only 1 or 2 feet thick occurs near
the middle of the member in several sections near the
Idaho-Wyoming border. Most sections contain minor
amounts of browni?h-red fine-grained sandstone interbedded with the red siltstone. Yellowish-white sandstone occurs locally at or near the base of the member.
The basal beds of the member may consist of red siltstone, of soft yellowish sandstone, or of brecciated limestone, and they invariably rest sharply on the hard
quartzitic Nugget sandstone. The upper contact of the
member is marked by an equally sharp change from
soft red siltstone to sandy or massive oolitic limestone.
Member B thickens westward from 25 to nearly
300 feet. In western Wyoming this member consists
mainly of medium- to thin-bedded, grayish-black to
dark brownish-gray limestone. Its basal unit generally
t
t
t
J ^
N T E R M O U N T A I N
0
A S S O C I A T I O N
consists oi 5 to 15.feet or more of dark oolite that contains a few sand grains and some pyrite. Thinner oolitic
beds occur higher in the formation in some sections.
In southeastern Idaho the basal 20 to 60 feet generally
consists of brownish, sandy, crossbedded limestone that
may contain tiny pebbles of red, green, and gray siliceous material. Similar sandy limestones also occur at
higher levels. Some of the sandy beds are'glauconitic.
Oolitic beds are generally present above the basal unit
of sandy limestone. A light-green to white volcanic
tuff (Mansfield, 1927, p. 97) from 5 to 10 feet diick
occurs within the member in the general area between
Cokeville and Afton, Wyo. The member has furnished
a large fauna of mollusks. Gryphaea planoconvexa
Whitfield is one of its most common and most characteristic fossils. The ammonites Stemmatoceras and
Chondroceras (Defonticeras) have been found in
most sections in the upper part of the member and
prove its middle Bajocian (earlier Middle Jurassic) age.
The member persists southward into north-central Utah
as least as far as Thistle. In the Uinta Mountains it is
recognizable as far east as Lake Fork but is absent on
the Whiterocks River. In the Jackson Hole area it thins
eastward and becomes shaly, but the basal oolitic unit
persists.
Member C thickens westward from 50 feet in western Wyoming to 350 feet in Idaho and consists mainly
of medium-gray shaly limestone that is very soft basally
but becomes harder upward, contains some thin beds
near its top, and grades into the overlying silty beds of
member D. A few thin beds near the top are generally
composed mainly of crinoidal fragments. It weathers
characteristically into light-gray splintery fragments.
Its basal contact is ttftnsitional within a few inches in
most sections. Its lower two-thirds has furnished Gryphaea planoconvexa Whitfield. The ammonites
Stemmatoceras and Chondroceras were found about
10 feet below the top of the rnember on the North Fork
of Stump Creek in the Freedom Quadrangle, Idaho.
These ammonites show that the member is of early
Middle Jurassic age. Member C is recognizable lithologically in northern Utah as far south as Thistle and
as fat east in the Uinta Mountains as the Whiterocks
River. It thins eastward rapidly in the Jackson Hole
area and is only about 50 feet thick at Lower Slide
Lake on the Gros "Ventre River.
Member D thickens generally westward from 35
feet in western Wyoming to 270 feet in Idaho but
varies considerably in thickness within short distances.
It consists of interbedded soft red, green, or yellow siltstone, silty to finely sandy yellowish limestone, and
greenish-gray silty shale. The limestones vary from
shaly to thick-bedded, frequently show crossbedding,
and contain marine fossils. Red siltstone dominates over
OF
PETROLEUM
GEOLOGISTS
55
limestone in the easternmost sections in Wyoming, but
westward the member becomes more calcareous, sandier,
and loses its red units. In Idaho is consists mostly of
yellowish limestone whose sandy members are cliffforming. In northern Utah, member D at most places
consists of a unit of yellowish sandy limestone overlain
• by a unit of soft red siltstone. The base of member D
is generally marked by a unit of silty to sandy limestone
that is transitional into the underlying member. The
top of member D makes a sharp contact with the overlying cliff-forming limestone at the base of member E.
Member E thickens westward from about 60 feet
in western Wyoming to 400 feet in Idaho. It consists
mostly of medium-gray to brownish-gray, mediumbedded, cliff-forming limestone but includes many thin
beds in its middle and upper parts. Most of the beds
are dense, but oolitic beds occur throughout. Generally
the basal bed is massive and oolitic. In Idaho, along
Preuss Creek and Stump Creek, some of the limestones
are slightly sandy. Member E is the main ridge-former
in the Twin Creek limestone and could be mapped
easily if detailed mapping of the Twin Creek is ever
found desirable. Its basal contact is sharp. It grades
into the overlying member through a unit of thinbedded to shaly limestone, and the boundary must generally be chosen arbitrarily within an interval of 30 to
50 feet. It has furnished very few fossils. Some of the
beds contain crinoid parts and Camptonectes. Gry. phaea nebrascensis Meek and Hayden was found near
the top of the member on Sliderock Creek and on Cottonwood Creek east of Smoot, Wyo. Member E is recognizable lithologically in northern Utah as far south as
Thistle and at least as far east as the Whiterocks River .
in the Uinta Mountains. The lowest few feet of limestone in the Carmel formation north of Vernal in sec.
26, T 3 S., R. 21 E., is probably the easternmost limit
of the member. Between the Whiterocks and Duchesne
Rivers the upper part of the member contains a thin
but conspicuous unit of grayish-white, thin-bedded,
nearly lithographic limestone. This limestone is overlain at Lake Fork by a few feet of sandy limestone.
Near Manila on the north side of the Uinta Mountains,
member E consists entirely of slightly sandy oolitic
limestone. Equivalent beds at Lower Slide Lake on the
Gros "Ventre River are about 57 feet thick and include,
from base to top, 20 feet of medium-bedded oolitic
limestone, 30 feet of shale with thin interbeds of limestone, and 7 feet of oolitic limestone. About 8 feet
above the base of the shale were obtained the ammonites Arcticoceras and Cadoceras. These genera are
common in the basal part of the Rierdon formation in
Montana and in equivalent beds in north<entral Wyoming.
WEST
EAST
I
BIG
ELK MOUNTAIN
NORTH
SIDE
SECe.T.ZS., R.45E.,
BONNEVILLE
CO., IDAHO
2 .
CABIN
CREEK
NORTH SIDE
3
MUMFORO
4
CREEK
NORTH SIDE
H08ACK
CANYON
5
GREEN RIVER
SECS.3I a32,T.39N.,RJI4W,.
SEC.I7,T.38N., R.I16W., SEC.32,T.38N.,H.I15W. SEC.6,T.58N.,R.n'JW.,TET0N
TETON CO., WYO.
6
LAKES
RED GRADE
T.39N.,R.I08W.ai09W. SECS.IZai3,T.5N.,R.6W.
SUBLETTE CO.,WYO.
FREMONT CO..WYO.
7
RED CREEK
SEC.r.T.GN., R.3 W.
FREMONT CO., WYO.
LINCOLN CO., WYO. S SUBLETTE COS., WYO. AFTER G.M.RICHMOND AFTER J.O.LJOVE ET AL AFTER J.O.LOVE ET AL
"UPPER
i l l ^ - ^ - r j SUNDANCE'FM.
PREUSS
SANDSTONE
r
»
z
z
c
>
O
z
z
COLUMNAR
SECTIONS ALONG
LINE A - A '
FIGURE 1.
fl-tl-HHH 11111111114^^
INTERMOUNTAIN
ASSOCIATION
OF
PETROLEUM
GEOLOGISTS
WEST
57
EAST
1
2
3
4
STUMP CREEK
COTTONWOOD CREEK
POKER FLAT
SOUTH PINEY CREEK
ON LANDER
CUT-OFF
EAST OF SMOOT
ON LANDER.CUT-OFF
NORTH SIDE
SECS.27a28,T6S., R.45E., SECS.35 a36,T.3IN.,R.II8W. SECS.3aiO,T29N..
SEC.II,T29N.,R.II5W.,
CARIBOU CO., IDAHO.
LINCOLN CO., WYO.
RJI7W.,UNC0LN CO.,WYO. SUBLETTE CO.,WYO.
PREUSS
LITHOLOGY
SANDSTONE
/^MEMBER G
CONGLOMERATE
MEMBER F
SANDSTONE
SHaLY
SANDSTONE
SILTSTONE
SHALE
LIMESTONE
SHALY
UI
z
o
IMEMBER E
<
ai
UJ
o
MEMBER 0 ;
MEMBER C
MEMBER 8
MEMBER A
'^
NUGGET SANDSTONE
I— 800
COLUMNAR
SECTIONS
FIGURE 2.
ALONG LINE
B-B'
EAST
1
MONKS
2
HOLLOW
S£C.32,T.4S.,R.5E,
AND
SEC.5,T.5S.,R:5E.,
UTAH
3
WEB'ER
RIVER*
NORTHWEST
OF
PEOA
4
DUCHESNE RIVER
SOUTH
SIDE
SECS.II 6 (4.,T.IS.,ft.5E,, S E C . 4 , T . I S . , R . 8 W . ,
CO., UTAH
SUMMIT
CO., U T A H
DUCHESNE CO,,UTAH
LAKE
ON
WEST
5
FORK
SIDE
S E C . Z . T . I N . , R. 5 W . ,
DUCHESNE
CO.j UTAH
PREUSS
M
•SANDSTONE ^
MEMBER G
WHITE
6
ROCKS CANYON
NW 1/4 SEC.tS a
SE 1/4
SEC.I8,T.2N.,R.1E.,
UINTAH
CO., UTAH
STEIN AKER
N.E, OF
DRAW
VERNAL
SEC.7,T.3!S.,R.22E.
UINTAH
CO., UTAH
ENTRADA
SAMDSTONE
Q
UJ
Z
o
*-
MEMBER F
>
z
z
V)
u
<
MEMBER E
ui
ui
cc
o
MEMBER D
z
n
O
Z
MEMBER C
3f
MEMBER B
.MEMBER A
NUGGET
SANDSTONE
zrt
CONGLOMERATE
•
T^T
.1
SANDSTONE
A^
SHALY
-1
SILTSTONE
SHALE
•
!•
SHALY
LIMESTONE
SANDY
:1 .'1;1
LIMESTONE
[ ->• 1 ^ A] A
BRECCIATED'
LIMESTONE
Win
GYPSUM
COLUMNAR
^EAsunen IN NE i/4
OF sec.i, T.IS ,ii.et.„
NORTHEAST OF OAKLEf
RED, MAROON,
PURPLE
I
SECTIONS ALONG
LINE
800
0-C'
FIGURE 3.
• • • • • • • • • • • • • • • • I H-S
(
m
N T E R M O U N T A I N
A S S O C I A T I O N
Member F thickens westward from about 250 feet
in western Wyoming to 1,600 feet or more in Idaho. It
is by far the thickest and most conspicuous part of the
Twin Creek limestone, forming extensive bare slopes
of light-gray color that are visible for great distances.
It consists mainly of soft, dense, light-gray shaly limestone that weathers generally into lighter-colored splintery fragments. At wide intervals the member contains
hard, diin beds that bear many fragrnents of crinoids
and echihoids, fairly well preserved Camptonectes, a
few oysters and belemnites, and rarely such pelecypods
as Pinna, Astarte, Isocyprina; and Trigonia. In the
middle' and upper parts of the member, some of the
thin limestone beds are oolitic, and others are silty to
sandy and ripple-matked. Eastward the member becomes less calcareous, and a few of the units weather
into chunky rather' than splintery fragments. Associated
with these chunky beds are some thin nodular limestones that may contain an abundance of Gryphaea
nebrascensis Meek and Hayden. Such fossiliferous
units are commori in the section on Greys River in the
Aftpn Quadrangle and on Cabin Creek and Tall Creek
in the Jackson Quadrangle. The member is overlain
trarisitionally by the silty to sandy beds of member G,
and the boundary inust be selected arbitrarily in most
sections. Member F Is. recognizable lithologically in
northern Utah as far south as Thistle but becomes much
shaliet southward, and some units are calcareous shales
rather than limestones (Baker, et al., 19^7). In the
Uinta Mountains, member F is typically developed as
far east as Lake Fork. At the Whiterocks River, and
eastward, the beds occupying the stratigraphic positipri
of member F consist mostly of redbeds and gypsum
that are customarily included in the Carmel formation.
Eastward, in the Jackson Hole area beyond the DarbyAbsaroka line of overthrusting, the beds equivalent to
member F consist- of thinner, mediumrgray, ealeareous
shales that hear their base in some sections contain a
few thin beds of nodular limestone. The nodular limestones contain a great variety of mdllusks, including the
ammonites Cadoceras and Xenocephalites. The shales
are especially characterized by an abundance of Gryphaea nebrascensis Meek and Hayden, whiGh cpntrasts
with the rarity of the species Ih the underlying oolitic,
limestones, that contain Arcticoceras. These shales are
lithologically and stratigraphically identical with the
.Rierdon formation of Montana. Eastward, in the Wind
River Basin, they pass into the Stockade Beaver shale
member of the Sundance formation.
Member G ran;ges in thickness from about 25 feet
to at least 288 feet, is highly variable in thickness, and
within the area of thrust faulting does not thicken appreciably in any direction. It consists mostly of yellowish to greenish, lavender, or pinkish, silty to finely
OF
PETROLEUM
GEOLOGISTS
5?
sandy, ripple-marked, thin-bedded limestone, and some
shaly limestone. Some units consist of medium-bedded
limestone that is generally oolitic or sandy. Some of
the sandy units are crossbedded. Many beds are a
Goquina of crinoid and echinold fragments, and their
upper surfaces are commonly matted with shells of
Camptonectes. The upper part of the member is generally harder and thieker-bedded than the lower part
and in places forms low cliffs. Westward, iri Idaho,
the meinber becomes sandier and consists of interbedded
units of ripple-marked sandy limestone and glauconitic,
thin- to thick-bedded sandstone. At Thomas Fork Canyon and Wolverine Canyon the member is more than
half sandstone and at Preuss Creek is mostly sandstone
(Imlay, 1952b, p. 1740). The sandy units are lithologically similar to the Stump sandstone. Member G is
overlain trahsitionally by red siltstone or sandstone at
the base of the Preuss sandstone. At the, top, in most
sections, is a transitional zone that Is generally less than
10 feet thick. In some sections, as on South Piney Creek
and On Cabin Creek in Wyoming, the transitional zone
is much thicker. In such sections the highest limestone
is arbitrarily placed in the Twin Creek, because a marine
limestone is apt to be more persistent than a red unit.
Member G is recognizable in Utah as far south as
Thistle and as far east as I^ke Fork. East of the Duchesne River the member consists mostly of greenishgray siltstone and sandstone, In the Jackson Hole area
it disappears eastward and is absent at Lower Slide Lake
on the Gros Ventre River, Member G is similar lithologically and stratigraphically to the Hulett sandstone
member of the Sundance formation in central and eastern Wyoming, weste;rn South Dakota, western NorthDakota, aiid southeastern Montana.
BIBLIOGRAPHY
Baker, A. A., et.al. ( 1 9 4 7 ) , "Stratigraphy of the Wajatch Mountains
in the Vicinity of Provo, Utah," U. S. GeoL Survey Preiitn. Chart
30, Oil and Gas Invest. Ser.
Imlay, R. W. (1950a) ,'"Jur3issic Rocki in the Mountains Along tKe
West Side of the Green River Basin," Wyoming Geological Assn.
Guidebook, Fifth Annual Field Conference, pp. 37-48, 3 figs.
....:
( 1 9 5 0 b ) , "Paleoecology of Jurassic Seas in the Western
Interior of the United States," Natl: Research Council, Report of
the Committee on a Treatise on Marine Ecology and Paleoecology,
19481949, no. .9, pp. 72-104, 8 figs., 1 correlation table.
,
{1952a), "Correlation of the Jurassic Formations of North
America Exclusive of Canada," Bull; Geol. Soc. Amer., Vol. 6 3 ,
pp. 953-992, 2 pis.
{1952b), "Marine Origin of the Preuss Sandstone of Idaho,
Wyoming, and Utah," Bull. Amer. Assoc. Petrol. Geol., Vol. 36.
• pp. 1735-1753, 4 figs.
Love, J. D.,iet al, ( 1 9 4 5 ) ; "Stratigraphic Sections and Thickness Maps
of Jurassic Roeks in Central Wyoming," U. S. Geol. Survey Prelim.
Chart 14, Oil and Gas Invest. Ser.
Mansfield, G. R. ( 1 9 2 7 ) , "Geography, Geology, and Mineral Resources ol Part of Southeastern Idaho," U, S. Geol, Survey Prof.
Paper 152, 409 pages, 46 figs., 63 pis.
Thomas, H. D., and Kruger, M, L ( 1 9 4 6 ) , "Late Paleozoic and Early
MesoJoic Stratigraphy of Uinta Mountains, Utah," Bull. Amer.
Assoc. PetroL GeoL, VoL 30, pp. 1255-1293, 10 figs.
Ar
F O U R T H
M>
A N N U A L .
F I E L D
LOCAL SECTIONS
r W l N CREEK LIMESTONE
Feet
Member B:
23. Limestone, medium-bedded, slightly sandy, crossbedded, medium yellowish-gray
22. Limestone, greenish-gray
21. Limestone, thin-bedded, yellowish- to pinkish-gray....
20. Limestone, medium- to thick-bedded, finely sandy,
crossbedded, medium-gray, weathers light brownishgray, traces of oysters
19. Covered
18. Limestone in beds 8 to 12 inches thick, very sandy,
a few small pebbles of red and yellow chert, crossbedded, dark brownish-gcay, weathers light-brown,
many oyster fragments in top bed
17. Sandstone, thin-bedded, crossbedded, fine-grained,
light-gray
16. Limestone, full of grit and small pebbles consisting
of red, yellow, gray and black chert and white quartz,
many sliell fragments
15. Covered
14. Limestone, thin-bedded, sandy, partly crossbedded, a
6-inch coquina bed about 5 feet below top, medium
yellowish-gray, weathers grayish-yellow
13. Limestone, thin-bedded, sandy, medium-gray, weathers
same
12. Limestone, thin- to medium-bedded, medium yellowish-gray, weathers brownish-gray
11. Limestone, sandy, hard, crossbedded, contains oysters,
bryozoans, and crinoid fragments
10. Limestone, finely sandy, partly crossbedded, mediumgray, weathers light yellowish-gray
-
1 9 5 3
22.
Lower part of Twin Creek limestone about IV2 miles
;ast of Bear Lake on road to Pegram in N W i 4 sec. 29 and
>JE14 sec. 30, T. 15 S., R. 45 E., Bear Lake County, Idaho:
Member C:
24. Limestone, shaly, soft, medium-gray, -weathers light'gray. Nor measured; at least several hundred feet
exposed
C O N F E R E N C E
?
30
1
20
5
11
6
5
1
44
37
32
14
IV^
22
Member A:
9. Mostly coveted. Some red siltstone occurs within
32 feet of top
130
8. Siltstone, light-red, soft
20
7. Siltstone, olive-green, soft
'.
7
6. Siltstone, light-red, soft
6
5. Limestone, light yellowish-gray, nodular
1
4. Siltstone, light-red to light-green
30
3. Limestone, medium- to thin-bedded, nodular and porous but not brecciated, light yellowish-gray to olivegray, weathers yellowish-gray
18
2. Limestone, thin-bedded, laminated, medium darkgray, weathers light-gray
2Vi
1. Siltstone, reddish-brown, soft
32
FGGET SANDSTONE.
Twin Creek limestone on north side of Preuss Creek
£1/4 sec. 15, T. 11 S., R. 45 E., Bear Lake County,
iho:
iUSS SANDSTONE.
IN CREEK LIMESTONE:
lember G :
Feet
25- Sandstone, thin-bedded; some sandy limestone, pinkish, weathers dull pinkish-gray, contact with Preuss
sandstone transitional within 10 feet
„
71
[ember F:
24. Limestone, shaly, soft, some thin beds, medium-gray,
• weathers light-gray. Cannot be measured because of
strong folding but at least
1,5004'ember E:
23- Limestone, medium- to thin-bedded, dense, mediumgray
95
Limestone, massive, slightly oolitic, some shell fragments, forms top of cliff
lo
21. Limestone, thin- to medium-bedded, slightTy sandy,
medium yellowish-gray
43
20. Covered
!...!.!!"! 26
19. Limestone, thick-bedded, cliff-forming, medium-gray.. 6I
18. Limestone, massive, oolitic, medium-gray
6
Member D :
17. Siltstone, brownish-red, soft
g
16. Limestone, thin-bedded to shaly, silty to sandy, light
yellowish-gray
33
Member C:
15. Limestone, shaly, soft, light-gtay, a few thin beds
271
Member B:
14. Limestone, medium- to thin-bedded, medium-gray,
forms low cliff
20
13. Limestone, thin-bedded, light-gray
21
12. Limeslone, thin- to medium-bedded, sandy, some
grains of grit size, brownish-gray
30
11. Tuff, dense, light-green to white
5
10. Covered
22
9. Limestone, thin- to medium-bedded, sandy, brownishgray, becomes less sandy toward base, some beds
coquinoid
Ill
8; Limestone, medium-bedded, gray
20
Member A:
7. Covered
6. Siltstone, brownish-red, soft
5. Limestone, brecciated, gray
4. Sandstone, thin-bedded, brownish-red, very finegrained
3. Siltstone, brownish-red, soft
2. Limestone, brecciated,'gray
1. Siltstone, brownish-red, soft
.-.
Approximate thickness
15
37
4
33
30
7
3
'..2,485 +
NUGGET SANDSTONE (not measured).
Twin Creek limestorie along old Lander Trail south
of Stump Creek in SVz sees. 27 and 28, T. 6 S., R. 45 E.,
Caribou County, Idaho (thicknesses approximate):
PREUSS SANDSTONE.
T W I N CREEK LIMESTONE:
Member G:
Feet
22. Limestone, thin-bedded, slightly sandy, yellowish- to
pinkish-gray, overlain by soft red siltstone at base
of Preuss sandstone
90
Member F:
21. Limestone, shaly, soft, light-gray
1,000±
Member E:
20. Limestone, medium- to thick-bedded, slightly sandy,
some beds oolitic, contains some comminuted shells,
medium-gray to light yellowish-brown
400
Member D :
19- Siltstone, brownish-red, soft
30
18. Limestone, thin-bedded, sandy, yellowish-gray
60
17. Limestone, cliff-forming, finely sandy, light yellowishgray, contains many small Gryphaea
20
16. Limestone, thin-bedded to shaly, silty, yellowish-gray 60
15. Limestone, cliff-forming, sandy, glauconitic, partly
oolitic, greenish- to pinkish-yellow
40
14. Limestone, thin-bedded to shaly, interbedded with
calcareous siltstone, some beds sandy, yellowish-gray.. 60
Member C:
13. Limestone, shaly, soft, light-gray, becoming harder
upwards, contains abundant Gryphaea planoconvexa Whitfield in its lower two-thirds
250
Member B:
12. Limestone, thin-bedded, slightly sandy, yellowishgray, weathers light yellowish-gray, upper 1 0 . ' * * '
contains many Gryphaea planoconvexa 'Whitfield..
.
60
f II
TABLE 1 .
a
THICKNESS IN FEET OF THE MEMBERS OF THE TWIN CREEK LIMESTONE AND
SOME EQUIVALENT FORMATIONS IN WYOMING, IDAHO, AND UTAH
Total
B
M o s q u i t o Pass, W y o . :
N'/i sec. 3 4 . T. 41 N . , R. 118 W
L o w e r Slide Lake, W y o . ;
Sec. 4 , T. 4 2 N . , R. 114 W
W o l v e r i n e C a n y o n , Idaho:
E'/4 sec. 2 8 & W'/a sec 2 7 , J . 1 S., R. 3 9 E
80
75
95
45
65
395
25
780
46
56
50
38
57
163
0
410
N O T EXPOSED
1500+
172
Fall Creek, I d a h o :
Sec. 1 8 , T. 1 N., R. 43 E
96
200
338
77
160
628
131
1630
Big Elk M o u n t a i n , I d a h o :
SWV^ sec. 6 , T. 2 5., R. 45 E
20
74
228
123
172
520
120
1257
Fall C r e e k , - W y o . :
NE'/i sec. 2 0 , T. 3 9 N., R. 116 W
43
55
151
40
69
477
48
903
C a b i n Creek, W y o . :
SVi sec. 1 7 . T. 38 N., R. 116 W
97
97
140
40
89
370
127
960
107
24
125
71
65
330
41.
763
76
60
104
43
65
290
28
666
223
281
250
270
400
1000
90
2514
M u m f o r d Creek. W y o . :
SE'/4 sec. 3 2 , T. 38 N.. R. 115 W
H o b a c k C a n y o n , W y o . : Sees. 31 & 3 2 ,
T. 3 9 N . , R. 114 W . ; sec. 6, L 3 8 N . , R. 1 1 4 W . . .
Stump Creek, Idaho:
516 sees. 2 7 & 2 8 , T. 6 S., R. 4 5 E
G r e y s River. W y o . :
Sec. 4 . T. 3 3 N . , R. 116 W
110
45
240
64
155
475
89
1178
C o t t o n v / o o d Creek. W y o . : WV6 sec. 3 6
a n d E'/j sec. 3 5 , T. 31 N., R. 118 W
102
87
275
66
146
530
100
1306
Poker Flat. W y o . :
Sees. 3 & 1 0 . T. 2 9 N., R. 117 W
125
88
247
83
175
813
102
1633
82
70
103
49
157
262
232
955
129
229
271
39
246
1500+
71
•2485
188
315
168
305
1625
111
2752+
140
91
252
115
400
575
86
1659.
75
79
245
69
218
735
102
1523
53
75
208
59
339
249
128
1111
150
85
275
75
154
1089
186
2014
77
68
184
35
212
487
177
1240
South Piney Creek, W y o . :
Sec. 1 1 , T. 2 9 N., R. 115 W
Preuss C r e e k . I d a h o :
E'/j sec. 1 5 , T. 11 S., R. 45 E
T h o m a s Fork C a n y o n , W y o . : Sees. 19 & 2 0 ,
T. 2 8 N . , R. 119 W., see. 2 4 , J . 28 N., R. 120 W...
Ferney G u l e h , W y o . : Sees. 1 & 2, T. 2 7 N . ,
R. 1 1 7 y j W . , see. 1 , T. 27 N., R. 118 W
Devils H o l e , N o r t h Fork, W y o . :
See. 1 5 . T. 2 7 N.. R. 117 W
LoBorge Creek, W y o . : NW'/4 see. 16 &
NE'4 see. 17, T. 27 N., R. 115 W
Sliderock Creek, W y o . :
See. 1 0 . T. 25 N., R. 118 W
Fontenelle Creek, South Fork, W y o . :
NW'/4 see. 3 3 , T. 26 N., R. 116 W
Leed C a n y o n , W y o . :
Sees. 1 8. 2 , T. 22 N., R. 119 W
40+
76
95
260
108
182
1118
102
1941
M a n i l a , W y o . (4 miles south o f ) :
SW'/i see. 6, T. 2 N., R. 2 0 E
0
0
24
7
23
227
50
331
W e b e r River near Peso. U t a h :
SWV4 sec. 11 & NW'/4 see. 14, T. 1 S.. R. 5 E
0
47+
125
107
220
776
82
Duchesne River. U t a h :
SW'/4 sec. 4 . T. 1 S.. R. 8 W
0
42
91
68
104
280
165
750
Lake Fork. U t a h :
Sec. 2 . L 1 N.. R. 5 W
0
32
109
30
]09
114
49
443
0
0
40
21
17
182
85
345
49
92
123
57
305
275
288
1189
71
183
41
345
?
?
W h i t e r o c k s River. U t a h :
NWV4 see. 19 & SE'/4 see. 1 8 . T. 2 N . , R. 1 E
Monks Hollow. Utah:
See. 3 2 . T. 4 S., R. 5 E.. & sec. 5. T. 5 S.. R. 5 E...
Thistle, U t a h :
WMi sec 33. T. 8 S.. R. 4 E
111
9
13574
5
I N T E R M O U N T A I N
A S S O C I A T I O N
11. Limestone, shaly, medium-gray, weathers light yellowish-gray, contains Stemmatoceras
10. Limestone, massive, dense, medium-gray, weathers
white
9. Limestone, thin- to medium-bedded, slightly sandy,
(Mlitic, brownish-gray, rather soft
8. Limestone, sandy, glauconitic, crossbedded, contaitis
small pebbles of gray and red chert, many oyster
and crinoid fragments, dark-gray, forms low cliffs....
7. Limestone, sandy, thin-bedded, dark yellowish-gray..
6. Limestone, sandy, oolitic, medium- to thick-bedded,
contains many oysters on bedding surfaces, dark-gray..
5. Limestone, sandy, thin-bedded, contains many oyster
and crinoid fragments, dark-gray
Member A:
4. Siltstone, light-gray to pink, interbedded with yellowish thin-bedded limestone that is locally brecciated
and honeycombed
3. Siltstone, brownish-red, soft, poorly exposed; some
beds of honeycombed limestone near base
2. Limestone, medium- to thin-bedded, medium-gray,
weathers light-gray; contains considerable brownishto reddish-gray chert as nodules, short, thin lenses,
and as granules; crinoid fragments abundant; some
beds sandy and crossbedded
1. Sandstone, fine-grained, and siltstone, brownish-red,
poorly exposed
Total thickness of Twin Creek
50
6
35
25
35
30
40
41
65
70
47
2,514±
Twin Creek limestone on north side of Big Elk Mountain between junction of Elk Creek and Bear Creek in
the SWV^ sec. 6, T. 2 S., R. 45 E., Bonneville County,
Idaho:
PREUSS SANDSTONE
T W I N CREEK LIMESTONE:
Member G:
Feet
12. Limestone, thin-bedded, silty to finely sandy, yellowish-gray, ripple-marked, locally crossbedded, up. per 16 feet contains interbeds of pink siltstone
120
Member F:
11. Limestone, shaly, soft, breaks into splintery fragments, light-gray, has thin beds of nodular limestone
every 10 to 15 feet. Gryphaea nebrascensis Meek
and Hayden noted at 250 and 410 feet above base.... 520
Member E:
10. Limestone, medium- to thin-bedded, cliff-forming,
medium-gray, dense to granular, some beds slightly
sandy and showing weak crossbedding. One 4-foot
bed of fx>litic limestone occurs about 72 feet above
base
172
Member D :
9. Limestone, shaly to thin-bedded, sandy, yellowish
8. Siltstone, light brownish-red, soft
7. Limestone, thick-bedded, sandy, yellowish
Limestone, medium- to thin-bedded, becoming
thicker-bedded upward, medium-gray to yellowishgray
15
24
25
59
Member C:
5. Limestone, shaly, soft, light-gray, weathers into
pencil-like fragments
168
4. Limestone, medium-bedded, dark-gray, slightly sandy,
contains many crinoid fragments
12
3. Limestone, shaly, light-gray, poorly exposed
48
Member B:
2. Limestone, medium-bedded, yellowish-gray, becomes
sandy in upper part
Member A:
1. Sandstone, fine-grained, and siltstone, brownish-red
to mottled gray and red; contains some beds of
honeycombed limestone at top, poorly exposed
Total thickness of Twin Creek
74
OF
PETROIEUM
GEOLOGISTS
61
Twin Creek limestone along Fall Creek in Irwin
Quadrangle, measured from center to southwest cornet
of sec. 18, T. 1 N., R. 43 E., Bonneville County, Idaho:
PREUSS SANDSTONE.
T W I N CREEK LIMESTONE:
Member G:
Feet
23. Sandstone, thin-bedded (Vi'inch to 4 inches thick),
light yellowish- to olive-gray, some glauconite
60
22. Limestone, medium- to thin-bedded ( 1 inch to 12
inches thick), medium yellowish-gray, mostly (x>litic,
some dense, silty to finely sandy, weathers yellowishgray, some beds full of crinoid columnals and arm
fragments, some glauconite
3
21. Limestone, shaly, light yellowish-gray
27
20. Limestone, same as unit 22
41
Member F:
19. Covered
80
18. Limestone, shaiy, medium-gray, weathers light-gray,
chunky to splintery
;
453
17. Limestone, thin-bedded to shaly, medium-gray
95
Member E:
16. Limestone, medium- to thick-bedded, medium-gray,
oolitic to dense, weathers medium-gray
160
Member D :
15. Siltstone, red, soft
45
14. Limestone, medium-bedded, silty, txjlitic in lower
part, medium to yellowish-gray, weathers mediumgray, upper part dense, slightly sandy throughout but
mostly sandy toward top
32
Member C:
13. Limestone, thin-bedded to shaly, medium-gray,
weathers light gray
117
12. Limestone, medium-bedded ( 6 to 8 inches), mediumgray, weathers light-gray
32
11. Limestone, shaly, medium-gray, weathers light-gray,
chunky, becomes harder toward top
189
Member B:
10. Limestone, thin- to medium-bedded, medium- to
light-gray, weathers light-gray, contains Gryphaea
planoconvexa Whitfield
13
9. Limestone, very sandy, crossbedded, brownish-gray,
weathers same, forms low cliff
11
8. Limestone, brownish-gray, slightly sandy, mediumto thick-bedded, weathers medium brownish-gray
32
7. Limestone, medium-bedded, medium-gray to yel- •
lowish-gray
l6
6. Limestone, silty, thick-bedded (6 to 24 inches thick),
light brownish-gray, weathers medium brownishgray, traces of crinoid columnals
21
5. Limestone, oolitic, medium-gray
10
4. Limestone, dense, thick-bedded, light-gray
10
3. Covered
:
45
2. Limestone, medium gray to grayish-black, dense,
medium- to thick-bedded, weathers dark-gray
42
Member A:
1. Siltstone, mostly brownish-red, upper 20 feet purplish, soft; rests sharply on Nugget sandstone
96
Total thickness of Twin Creek
1,630
NUGGET SANDSTONE.
Twin Creek limestone and Preuss sandstone on Cabi
Creek, Jackson Quadrangle, in SVi sec. 17, T. .38 N., F
116 W., Teton County, W y e :
STUMP SANDSTONE (not measured).
PREUSS SANDSTONE:
Fee
20
1,257
29. Sandstone, dull-red to pink, thin-bedded to shaly,
fine-grained, rather soft, contains a few hard, thin
beds overlain sharply by glauconitic sandstone of
Smmp
28. Sandstone, massive, fine-grained, hard, light pinkishgray, weathers darker
62
6
F O U R T H
A N N U A L
27. Sandstone, dull-red, rather soft, a few hard layers
26. Sandstone, massive, very fine-grained, dull-pink,
cliff-forming
ELD
20
21
7IN CREEK LIMESTONE:
Member G :
25. Limestone, sandy, crossbedded, beds 1 to 3 feet thick,
light yellowish-gray, cliff-forming
17
24. Siltstone, shaly, mostly brownish-red, some yellowishgray
11
23. Siltstone, shaly, calcareous, ribboned yellow and gray. 16
22. Limestone, thick-bedded, finely sandy, shows some
crossbedding, light yellowish-gray, cliff-forming
4
21. Limestone, shaly to thin-bedded, silty, light yellowishgray
-•
48
20. Limestone, medium-bedded, consists mainly of crinoid and echinoid fragments, medium-gray
1 to 6
19. Limestone, shaly, medium-gray, weathers into lightgray splinters
16
18. Limestone, medium-bedded, sandy, medium yellowish-gray,' forms ledge
5
17. Limestone, thin-bedded to shaly, silty, yellowish-gray
Vlember F:
16. Limestone, shaly, medium- to light-gray, weathers
into light-gray splinters
253
15. Limestone, silty, yellowish
10
14. Limestone, shaly, fissile to splintery, medium-gray.... 32
13. Limestone, shaly, chunky, medium-gray
. 75
VIember E:
12. Limestone, medium- to thin-bedded, partly oolitic,
medium-gray
11
I I . Limestone, thin-bedded to shaly, poorly exposed
53
10. Limestone, medium- to thin-bedded, oolitic to dense,
medium-gray
25
klember D :
9. Siltstone, red, soft, upper contact sharp
40
klember C:
8. Limeslone, thin- to medium-bedded, silty, some beds
(Xilitic, medium yellowish-gray
10
7. Limestone, shaly, soft at base, forms low ledges at
top, medium-gray
130
«fember B:
6. Limestone, thin-bedded to shaly, medium-gray, Gryphaea planoconvexa Whitfield found at top
70
5. Limestone, oolitic, medium-bedded, slightly sandy,
dark-gray
11
4. Limestone, medium-bedded, dense, medium-gray
16
-lember A:
3. Siltstone, red, soft, poorly exposed
55
2. Limestone, medium-bedded, granular, light-gray, contains some chert
10
1. Limestone, brecciated, medium-gray, lower 2 feet
yellow
32
Total thickness of Twin Creek
960
GGET SANDSTONE.
Incomplete section of Twin Creek limestone on north
ik of Williams Creek in SWA sec. 12, T. 2 S., R. 39 E.,
igham County, Idaho:
Feet
'IN CREEK LIMESTONE:
dember B ( ? ) :
10. Limestone, oolitic, massive, sandy
15
9. Limestone, sandy, crossbedded, partly oolitic
60
(lember A:
8. Covered. Some float of soft red sandstone
100±
7. Limestone, medium- to thin-bedded, dense, mediumto dark-gray, siliceous, contains brownish chert
nodules
20
6. Limestone, yellowish-gray, brecciated or honeycombed
20
5. Limestone, medium- to thin-bedded, dense, mediumto dark-gray, siliceous, contains some brownish chert
nodules
140
4. Limestone, brecciated, light yellowish-gray
8
3. Limestone, finely sandy, light yellowish-gray, interbedded with brownish-red siltstone
6
C O N F E R E N C E
—
1 9 5 3
2. Siltstone, soft, dull-red, yellow, green, some interbedded honeycombed limestone
20
1. Siltstone, soft, pink to dull-red, some iigiit-green
or yellow, mostly non-calcareous, contains some beds
of dull-red to yellow, fine-grained, non-calcareous
sandstone; about 30 feet below top occurs 2 feet of
dense, shaly yellow limestone
lOO
NUGGET SANDSTONE.
Twin Creek limestone equivalents north of Lower
Slide Lake on Gros Ventre River in sec. 4, T. 42 N.,
R. 114 W., Teton County Wyo.:
Feet
PREUSS SANDSTONE ( ? ) (may be basal Stump):
24. Siltstone, red
23. Sandstone, light-gray
3
5
T W I N CREEK LIMESTONE EQUIVALENTS:
Member F:
22. Shale, calcareous, medium-gray, weathers light-gray,
one thin bed of nodular limestone in lower foot,
several thin beds of fossiliferous limestone from 35
to 40 feet above base include Cadoceras and Xenocephalites.
Gryphaea
nebrascensis
abundant
throughout
163
Member E:
21. Limestone, cxilitic, thick-bedded at top and bottom,
thin-bedded in middle, medium yellowish-gray
7
20. Shale, calcareous, medium-gray, weathers light-gray.
Gryphaea nebrascensis obtained 10 feet below top
(lowest occurrence noted)
20
19. Shale, calcareous, medium-gray, and thin beds of
soft, brownish-gray limestone, weathers light-gray.
Eight feet above base occur Artrticoceras, Cadoceras,
and many pelecypods
10
18. Limestone, oolitic, massive, medium-gray, weathers
same
3Vi
17. Limestone, medium- to thin-bedded, slightly fx>litic,
crumbly, medium yellowish-gray, weathers mediumgray, very fossiliferous
.'.
4Vi
16. Limestone, medium- to thick-bedded, beds 6 to 12
inches thick, (X>litic, hard, medium yellowish-gray,
weathers medium-gray, traces of fossils
•.
12
Member D :
15. Limestone, shaly, soft, yellowish-gray
5Vi
14. Limestone, shaly, soft, olive-green to yellowish-gray..
1 Vi
13- Siltstone, brownish-red, soft, makes sharp contact
with underlying unit, thickens westward in Vi mile
to 43 feet
33
Member C:
12. Limestone, shaly, medium-gray, contains a few thin
beds of coquinoid limestone and locally a hard bed
of coquina at top
23
11. Limestone, shaly, soft, medium-gray, weathers same.. 27
Member B:
10. Limestone, mostly shaly, fairly soft, some beds from
4 to 10 inches thick at intervals of 4 to 8 feet, darkgray to grayish-black, weathers dark-gray; 20 feet
above base occurs Chondroceras; Gryphaea planoconvexa Whitfield occurs throughout
35
9. Limestone, medium- to thin-bedded, mostly dense,
partly oolitic, upper 2 feet slightly sandy and pyritic,
medium yellowish-gray, weathers medium-gray
16
8. Limestone, shaly, soft, medium-gray
4
7. Shale, soft, yellowish-gray
1
Member A;
6. Siltstone, brownish-red, soft
15
5. Limestone, pinkish-yellow, weathers pinkish to yellow, forms top of cliff
'8
4. Limestone, brecciated, gray to yellow, angular fragments as much as a foot in diameter but most fragments smaller, forms cliff
16
3. Limestone, brecciated, silty, purplish to yellow and
gray
2±
2. Limestone, silty, soft, yellow to pinkish
1 to 2
1. Siltstone, brownish-red, soft, rests sharply on Nugget
sandstone
3
Total thickness of Twin Creek
410
!
.v-
* t
vlt- F O U R T H
A N N U A L
FIELD
C O N F E R E N C E
-
1 9 5 3
AREA
USwest AISSISSIPPIAN STRATIGRAPHY IN THE UTAH-IDAHO-
Misf
WYOMING AREA
mmmvi OF mm
By F. D. HOLLAND, JR.
Curator, University of Cincinnati Museum
RESEARCH SfiSTltHTS
EARTH S C i l M e i
INTRODUCTION
Mississippian seas were widespread in the Rocky
[ountain region, and throughout most of Mississippian
me broad seaways extended from Alaska to Mexico.
Zithin these seas thick sequences of limestone, sandone, and shale were deposited, with carbonate rocks
redominating in volume and extent. Eardley (1949,
, 665) has given the name "the Madison basin" to
long narrow zone extending from western Montana,
irough southeastern Idaho, and into southern Nevada,
hich received over 4,000 feet of sediments in Lower
fississippian time. A somewhat smaller area in westn Utah and central Idaho which sank over 6,000 feet
id received over 6,000 feet of sediments in the Misssippian is called "the Brazer basin."
The area covered by the excursion (Ogden, Utah,
Jackson, Wyoming) (Figure 1) lies roughly along
bat Kay (1951, p. 10, 14) has called "the Wasatch
le." This hypothetical line roughly marks the posiin of the monoclinal flexure from the traton on the
5t into the miogeosyncline on the west. The area of
; miogeosyncline west of the Wasatch line (defined
a line of disappearance of the Lower Cambrian and
; 2,000 foot isopach of the entire Cambrian) has
:n termed the Millard Belt (Kay, 1947, 1951). Thus
• tectonic pattern in the Cordilleran region was set
Cambrian time and the same pattern was followed
oughout the Paleozoic. Kay (1951, p. 14) says,
stems from the Ordovician through the Jurassic are
erally more. fully represented and thicker in the
le areas in which lower Cambrian is present and
whole Cambrian thicker."
The route of the trip throughout most of its extent
far enough west so that practically the maximum
ion of Mississippian is seen. Thus, thick fossiliferous
iissippian limestones in the Logan-Ogden area pass
vard into drab sandstones, with the fossiliferous
stones dropping out as the crato'n is approached.
Brush Creek in the Uinta Mountains, Williams
13, p. 609) has stated that the Madison formation
sists essentially of light-drab sandstones and silt;s, with tongues of red beds and a thick member of
formational breccia," Also Wanless, et al. (1946)
reported progressive westward thickening of the
ssippian .from 1,080 feet in the Gros Ventre
e of western Wyoming, to 1,800 feet in the
; River Range of eastern Idaho; further west-
ward in Idaho the Mississippian passes into a thick geosyndinal black shale sequence. Two formations make
up the Mississippian column in most of the area: the
Madison limestone (Kinderhookian) below, overlain
unconformably by the Brazer limestone (Meramecian
and Chesterian) above. A thin unit of shale, the
Leatham formation (lower Kinderhookian), is known
to conformably underlie the Madison in the Logan,
Utah area; however the extent of this shale outside
of the Logan area has not yet been determined by field
studies.
The Mississippian generally rests unconformably
upon the Devonian Jefferson limestone or an equivalent of the Upper Devonian Three Forks formation. In
much of the area the Upper Mississippian Brazer limestone is unconformably overlain by the Pennsylvanian
Wells formation, but from Teton Pass eastward the
Darwin sandstone member of the Amsden formation
(Lower Pennsylvanian age) overlies the Brazer.
The first report of Carboniferous rocks in Utah
was by the Stansbury expedition in 1849 (Stansbury,
1852). Hayden, Peale, and others made observations
in the Logan area. King (1876, p. 478-80) first named
the strata, calling them the "Wahsatch" limestones of
"Devonian" and "Carboniferous" age, however, Richardson (1913) revealed that King's "Wahsatch" included rocks of Ordovician to Mississippian age. The »
term Wasatch has not since been used to refer to
Paleozoic rocks.
.
The type sections of two of the Mississippian for-ff;l^
mations lie near the route of the field trip. Richardson
in 1913 named the Brazer limestone from exposures in
Brazer Canyon in the Crawford Mountains, 6 miles
northeast of Randolph, Utah; and Holland (1952,
1719) named the Leatham formation for the exposi
on the north wall of Leatham Hollow about 8 air-Ii
miles southeast of Logan, Utah. The Madison wif
named by Peale (1893) who failed to designate o^i
locality for the Madison limestone but did implj^^
the unit was named for the Madison River in cbc,
Forks, Montana area. Sloss and Hamblin
Holland (1952) have discussed the compl|g
of the name Madison and have described J n
section directly north of Logan, Montan^
this the type section of the.Madison.
i
-f'
^
I N T E R M O U N T A I N
A S S O C I A T I O N
OF
PETROIEUM
FIGURE 1.-GENERAL LOCATION MAP
GEOLOGISTS
33
-»'"
34
F O U R T H
A N N U A L
FIELD
Mansfield (1927) prepared a comprehensive report on the geology of southeastern Idaho and included
in this report a description of the Carboniferous and
Triassic fossils by Girty (1927, p! 411-46). Richardson (1941) published a report on the geology of
the Randolph Quadrangle (next quadrangle east of
the Logan Quadrangle) and included a geologic map.
Williams (1943) has described numerous sections of
Carboniferous formations in the Uinta and Wasatch
Mountains. Eardley (1944) studied the geology of the
north-central Wasatch Mountains, and Williams and
Yolton (1945) described in detail Brazer and Wells
seaions near Dry Lake, southwest of Logan, Utah.
Parks .(1949 and 1951) zoned the Brazer on the basis
of its coral fauna and Williams (1948) summarized
much work in the Logan Quadrangle and presented an
excellent report on the stratigraphy, structure, and
historical geology, with a geologic map and detailed
cross-sections.
Kirkham (1924) discussed the geology and mapped a large portion of the Caribou Range southwest of
Swan Valley, Idaho.
C O N F E R E N C E
—
19 5 3
In the mountain ranges about the Jackson Hole
region the writer has relied principally upon reports
by Horberg (1938), Horberg, Nelson, and Church
(1949), Thomas (1948), Wanless and others (1945,
1946).
r
r
I
I I
\
Ogden to Montpelier — East of Ogden the Mississippian crops out in Ogden Canyon. There the darkgray, thin-bedded typical Madison is about 600 feet
thick, and the Brazer is only about half as thick (1,100
feet) as in the Logan area.
Mississippian strata are not again encountered until
Wellsville Mountain and the Pisgah Hills southwest
of Logan. Approaching Dry Lake from the south the
Leatham and Madison are not exposed along U. S.
Highway 91- A very thick section of Brazer is, however, exposed along a road cut of an old portion of
U. S. Highway 91 where it turns eastward across the
Pisgah Hills toward Sardine Canyon. Williams and
Yolton (1945) have reported 3,700 feet exposed in
the Dry Lake section but this is over 1,000 feet more
than was measured by Parks (1949). The former have
listed over 130 species from the most typical strata of
^^^^H
FIGURE 2.—Mississippian section on the east slope of Beirdneau Peak viewed
from U. S. Highway 89 about 5 miles east of mouth of. Logan Canyon, Utah.
N T E R M O U N T A I N
'[|
A S S O C I A T I O N
the formation, the thin- to medium-bedded, dark-gray
to grayish-black cherry limestones of the middle Brazer.
Caninia, other large tetracorals, Lithostrotion whitneyi Meek, Spirifer brazerianus Girty, and Chonetes
are abundant and frequently excellently preserved;
many specimens are silicified and suitable for acid
etching.
Entering Logan Canyon east of Logan one can see
the cliffs of nearly flat-lying resistant Mississippian
limestones near the axis of the Logan syncline. About
5 miles from the mouth of the canyon an excellent
view of the entire Mississippian section is obtained from
the road (Figure 2 ) .
There on the east slope of Beirdneau Peak the
Upper Devonian "Contact Ledge" can be seen as a thin
zone of resistant limestone marking the top of the
Devonian section. Above this, a slope is formed on
the Lower Mississippian Leatham formation (about 75
feet thick). The Leatham consists of shales, sandy
shales, and dark reddish-gray, nodular limestones characterized by abundant nodules 1 to 2 inches in diameter
containing Rhipidomella missouriensis (Swallow)
and Syringothyris. At the type section in Leatham
Hollow, about 9 miles to the south, the base is marked
by a 3-inch conglomeratic limestone, bearing angular
chert nodules, limestone pebbles, and an occasional
fragmental fish tooth.
Above the Leatham the Madison limestone rises
in a sheer cliff, locally known as the "Chinese Wall".
This part of the Madison is about 250 feet thick, and is
composed of dark-gray, fine-crystalline limestone
rhythmically interbedded with thin shaly limestone
beds. A long steep slope rises to the base of a second
cliff of the Madison, which may be termed the "Upper
Chinese Wall". This middle slope of the Madison
is formed on dark-gray, fine<rystalline to sublithographic, thinly-bedded limestone rhythmically interbedded with l^-inch beds of grayish-orange, soft, silty
to argillaceous limestone. The lithologic character of
most of the "Upper Chinese Wall" resembles that of
the slope below, but this part appears to be more resistant to weathering and erosion. At several levels,
benches or reentrants are weathered into the cliff,
so that this upper cliff is not as well-defined as the
lower cliff of the Madison. This thin-bedded limestone is the lithologic and faunal equivalent of the
Lodgepole limestone of the Logan, Montana area.
Osagian elements are in general lacking from the
fauna. Whether never deposited, or removed by erosion, there does not seem to be an equivalent of the
thick-bedded Mission Canyon portion of the Madison
of Montana present in this area. The fauna of the
OF
PETROLEUM
GEOLOGISTS
35
Madison is characterized by tetracorals of smaller size
than those of the Brazer, abundant Syringopora, Spirifer cf. S. centronatus, and abundant gastropods and
cactocrinids.
• Locally the base of the Brazer is marked by a phosphatic shale member which seems to have been deposited on the eroded upper Madison surface. Williams
(1939, 1943, p. 595) has reported this basal phosphatic shale in Blacksmith Fork Canyon but it is miss
ing in Leatham Hollow, 2 miles to the north. Williams (1943, p. 611) mentions the variety of lithologic types in the various exposures of Brazer, but
says that each section generally contains some intercalated limestone and sandstone and generally some
pure thick-bedded limestones (note cliffs near the top
of Beirdneau Peak, Figure 2). The Wells is not exposed
on the north side of Logan Canyon but appears in an
incomplete section atop Logan and Millville Peaks, the
high peaks just east of the town of Logan and south
of lower Logan Canyon.
Steeply tilted Madison beds crop our in several
small areas south and east of Laketown in the Randolph Quadrangle, and rhen disappear under the cover
of the Wasatch formation. The Brazer also outcrops
about a mile east of Laketown with a bed of phosphate
rock near the base.
From Sage Creek Junction the escarpment of the
Crawford Mountains can be seen to the southeast. The
Brazer forms this scarp, and here the Madison forms
the upper slopes and the crest of the mountains. The
200 feet (or at least the upper portion) of the "thinbedded impure earthy-gray limestone, which weathers
to yellowish and reddish tints" reported by Richardson
(1941, p. 20) to underlie conformably the Madison
in the Crawford Mountains probably represents the
Leatham formation. The Brazer type section in this
area has been restudied by Williams (1943, p. 610)
who states that neither the top nor the bottom is exposed, and that the limestones are dolomitized. Mississippian fossils are rare and poorly preserved in rhe area.
Montpelier Through Georgetown Canyon and
Return. — The large fault block that rises norrheast of
Montpelier is composed of Madison limestone. Brazer
limestone is present on the west slope of the hills just
east of town, but in this area the Mississippian is faulted
and the section is incomplete.
The Mississippian is next seen in a broad strip along
the west side of Crow Creek; the outcrop of the Brazer
limestone is crossed at the entrance to Wells Canyon.
At the mouth of Wells Canyon a partial section (the
base is covered by hill wash on the east) of Brazer was
F O U R T H
A N N UAL
FIELD
reported by Mansfield (1927, p. 63) as 1,130 feet
thick. The section dips westward into the Webster syncline of Mansfield which is marked by the Pruess
Range, One-foot to three-foot beds of dark-gray limestone mark the lower part of the section here, with
whitish sandstones and light sandstones exposed above.
In' this seaioti shaly, cherty, limestone marks the top
of the Brazer, underneath sandstone of the basal Wells
formation,
Brazer beds of essentially the same lithology form,,
the crest of anticlinal Snowdrift Mountain, and the
route passes through it along the South Fork of Deer
Creek.
Although Madison, is not exposed in the. Crow
Creek Quadrangle, it crops out at a number of places
in the Slug Creek Quadrangle to the west. The high
ridge west of Georgetown Canyon is formed by a large
porrion of Madison brought up by faulting. The Brazer
is lower on the canyon walls and the trip crosses a
narrow slice, dipping 75° west, brought up by a thrust
subordinate to the main overthrust.
A spectacular portal or gateway at the' mouth of
Georgetown Canyon is formed by ledges of Madison
limestone.
Alpine, Idaho, to Jackson, Wyoming. — The
Madison and Brazer limestones make up the rugged
mountains along the northeast edge of the Sriake River
Valley from Alpine • to Swan Valley; Idaho.
West of the Snake River only one sefctibn of Madison is crossed by the route and this lies at the entrance
to Fall Creek Canyon. Here in the Fall Creek Quadrangle, however, the Brazer is well exposed along the
west side of the Snake River fault, and a complete
'section is obtained in Fall Creek Canyon. South of
Fall Creek' the Brazer runs alon^ the axis of the Snake
River anticline (Kirkham, 1924). In this area the
Madison and Brazer are each about 1,000 feet thick.
Each are cliff-raakefs but the Brazer is again the, more;
massive, and although each is dominantly made up of
dark-gray, fine- to coarse-crystalline limestone, the
Brazer again weathers to the lighter color, being lightgray or almost white. As in the Utah area the faunas
df both formations are dominated by rugose corals,
those.in the Brazer being much larger, generally 3 to 8
inches long.
Along Pine. Creek, west of the fault, typical Madison
and Brazer are exposed. In the west part of the canyon
the beds dip about 25" to the west', but farther eastward dips as high as 75° are encountered near the main
"ault.
Ea^t of Victor, CairboniferGus lirriestohes rise from
mder the cover of Mesozoic and Cenozoic sediments
)f the Teton Basin to focm the gently-dipping western
lope of the. Tetons. Horberg (1938, p. 16) states
C O N F E R E N C E
-
19
5;3
that -'the tabular inter-stream areas and most of the
irnportant sedimentary peaks (Mt. Hunt, 10,775 feet,
Rendezvous Peak, 10,924 feet, and Fossil Mt., 10,553
feet) are formed of these [Madison .and Brazer] limestones." The Madison and. Brazer forrn the bulk oi
the mountain just north of Tetoh Pass. Here the Brazer
has thinned considerably and is subordinate to the
Madison. In general the disringuishing chatacterisrics
of the limestones are the same in this area as in areas
to the south.
Thomas (1948) states that Bachrach (1946) has
recognized the Brazer over a wide area in the Hoback
and Gros Ventre Mountains with the Darwin sandstone
everywhere present above the Brazer. Thornas considers the Darwin as basal Pennsylvanian in this area.
The Gros Ventre Buttes northwe'st of Jackson are
similar to each other in structure and composition.
They represent normal fault blocks of gently-dipping
Paleozoic strata and younger lava flows tilted westward
along their eastern .scarp slopes. The Madison crops
gut on the, southeast corner of each of the buttes and
Horberg (.1938, p. 42) reports that =;a-tunnel dug west
of Jackson on East Gros Ventre Butte has penetrated
the talus and exposed the slickehsided, polished surface
of Madison limestone forming the footwall in contact
with breccia and talus on the east.
Two smaller buttes south of the main Gros Ventre
buttes expose Madison limestone (and other Paleozoics) as remnants of'the southwest-dipping Jackson
thrust plane.
ACKNOWLEDGMENTS
I wish to thank Mr. J. B. Pogue of the Departinent
of Geology and Geography, University of Cincinnati,
for his critical reading of the manuscript and for his'
suggestions. I also thank my wife, Margine, for typing
the manuscript and for other aid,
SELECTED REFERENCES
Bachrach, Ruth ( 1 9 4 6 ) , "Gotrelation bf Mississippian and Pennsylvanian Strata in Lincbtn, Sublette and Tetph Counties, Wyomingi"
Unpublished Master's Thesis, Univ. of MicHigah.
Eardley, A. J. ( 1 9 4 9 ) , "Paleotectonics and Palepgeolbgic Maps df
Central and Wesrern North America," Bull. Amer. Assoc. Petrol.
Gebl., vol. 33, no. 5, pp. 655-82,
Girty, G. H. ( 1 9 2 7 ) , "Descriptions of New Species of Carbon iferous
and Triassic Fossils," in. Mansfield, G. K.., "Geographj', Geology,
and Mineral Resources of Partof SputKeastern Idaho," U. S. Geol.
- Survey Prof. Paper 152, Appendix.
• .
Holland,, F. D,, Jr. (1:952), "Stratigraphic Details of Lower Mississippian Rocks in Northeastern Utah and Southwestern Montana,"
Bull. Amer. Assoc. Pettpl_. Geol., vol. 36, no. 9. pp. 1697-1734.
Horberg,-Leiand ( 1 9 3 8 ) , "The Structural Geology arid Physiojgraphy
of the Teton Pass Area, Wyoming," Augusrana library Pub. 16;
86 pp, 2 figs.
..., Nelson, Vintrent,, and Church, Victor ( 1 9 4 9 ) , "Structural
Trends ih Genti^l Western Wyoming," Bull. Geo). Soc. America, vol. ,60, pp; 183-216, 4'figs., 6 pis.
Kay, Marshal] ( 1 9 5 1 ) , "North American Geosynclines," Geol. Soc.
America Mem. 48, 143 pp., 20 figs., I6 pls:
I
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I
I
ODIVERSITY OF UTAH
RESEARCH INSTITUTE
EARTH SBiEN8E>kAB.
28
Ir
FIELD
C O N F E R E N C E
-
r
1 9 5 3
REGIONAL STRATIGRAPHY OF THE DEVONIAN SYSTEM IN
NORTHEASTERN UTAH, SOUTHEASTERN IDAHO,
AND WESTERN WYOMING
Sswest
^y J ^ ^ ^ ^; BROOKS
^.{.pg^
Southern Methodist University, Dallas, Texas
Devon
and
I
I
J O H N M. ANDRICHUK
Gulf Oil Corporation, Tulsa, Oklahoma
STRATIGRAPHY
Figure 3 shows a cross-section of Devonian rocks
extending from sourhwesternmost Montana and immediately adjacent Idaho eastward to western Wyoming
(Cody area, Wind River Range, and Teton Range) and
thus southwestward to norrheastern Utah.
In northern and northeastern Utah relatively
rapid thinning with correspondingly rapid changes in
vertical stratigraphic sequence characterize rocks of
Devonian age. The thickest portion of the Devonian,
as exposed in Logan Canyon (Section 8, Figure 3), is
composed of three stratigraphic units described in derail
* by Williams (1948). The units are, from bottom to
^ top, the Water Canyon formation, a light-gray to almost
white, coarsely-crystalline, sandy, dolomitic limestone,
the Hyrum member of the Jefferson formation, a drab,
dark-gray, mediuum- to coarsely-crystalline secondary
dolomite, and the Beirdneau member of the Jefferson
formation, a light-tan to buff unit composed of platy
beds of siltstone and' dolomite with partings of tan
shale being prominenr throughout the sequence (Fig-
FIGURE 1.—South wall Logan Canyon east of Logan, Utah.
Massive cliffs on upper wall are Madison limestone,
^ l o p e - m a k i n g sequence to lower, less well developed
'cliffs is Beirdneau member, Jefferson formation. Lower
cliffs mark upper portion of Hyrum member, Jefferson
formation.
ure 1). Local zones of sedimentary breccia are prominent in some parts of the section. The Beirdneau member exposed in Logan Canyon is some 400 feet thick.
Holland (1952), describing what is apparently the
uppermost portion of this unit, exposed a few miles
south of Logan Canyon in Leatham Hollow, has
measured a thickness of some 70' of rocks of similar
lithology to which he assigns a Kinderhookian age and
which he correlates with the Sappington sandstone of
southwestern Montana. In Leatham Hollow this unit,
named the Leatham formation by Holland, rests disconformably on the dark-gray limestones and dolomites
of the Jefferson formation (presumably the Hyrum
member of the Jefferson of Williams in Logan Canyon). Absence of so great a thickness, in view of its
presence a few miles to the north seems somewhat
anomalous. However, since the writers have not visited
the Leatham Hollow area they do not presume to offer
an explanation of the apparent anomaly.
The Water Canyon formation at the base of the
sequence is not recognized elsewhere in the area of the
field trip. However to the south and west, in central
Utah, correlable units are exposed. The Hyrum member of the Jefferson is likely correlative with the Jefperson formation which lies ar the base of the Devonian section in areas to the north, east, and south. The
Beirdiieau member of the Jefferson formation may be
chronologically a close correlative of the Three Forks
formarion, recognized elsewhere in the region. However, the lithologies are similar only in that both repre-,
sent a change in late Devonian time from purely car- ^^
bonate deposition to that of a more clastic nature.
To the east (Laketown-Randolph area, seaion 7 , ^ ^
Figure 3) two units of Devonian age are recognized;
The Jefferson formation, a dark- to medium-gray, i n ^
dium- ro coarsely-crystalline unit composed of varying
beds of limestone and secondary dolomite is conform
ably overlain by the Three Forks formation w h i d i ^ ^
sists of a shaley, very thinly-bedded, olive-gray I'ma^gjg
typically making a topographic saddle in areas rf„d^
ping beds and almosr always charanerized by , a t ^ ^ ^
weathering zone at the outcrop surface ( F ' f i J ^ ^
WKl
f
(
J
1
INTE.RMOUNTAIN
A S S O C I A T I O N
the south at Durst Mountain (Section 9, Figure 3) eastof. Ogden, Utah, the Devonian is represented by the
Three Forks formation which is composed predominantly of limey and sandy shales which are oIi.ve to buff in
color and which show the red soil weathering, zone
typical of the Three' Forks at other localities.
FIGURE 2.—North wall Laketown Canyon, east of Laketown, Utah. Saddle in ridge crest to left of center is
typical of Three Forks formation. Units to right are
Mississippian limestones. Strata to left of saddle are
uppermost Jefferson formation.
Still farther to the south in the vicinity of Oa:kley,
Utah (Section 10, Figure 3) Devonian rocks are represented by a very thin section of tan calcareous shales
and siltsones which rests disconformably on a quartzite
of questionably Cambrian age and which apparently
grade upward into rocks of Mississippian age. A formation name has not been assigned to these rocks, but
presumably they are genetically related to the Three
Forks formation mentioned to the north, representing
a slightly variant shelf environment. A fauna of Hackberry age is present In these beds. This section is the
most eastward exposure of Devonian rocks sp far noted
in Utah and, in view of the thinness and .clastic nature
of the sediments, presumably represents deposition not
too far removed from the zero edge to the east.
In Wyoming, the Devonian interval is termed the
"Darby formaiiion", but approximate lithologic equivalents of the Three Forks-Jefferson may be differentiated. The upper part of the Darby sequence is characterized by conspicuous amounts of elastics (sand, silt,
and argillaceous material) iriterbedded with the carbonates and may be correlated with the Three Forks.
The remaining lower relatively pure carbonate !beds
are considered Jefferson equivalents. Eastward in the
shelf area of Wyoming, this Jefferson interval thins
and Is not recognizable near the eastern zero edge. The
Three Forks beds appear to be transgressive eastward
in Wyoming.
OF
PETROLEUM
GEOLOGISTS
29
In southwestern Montana and adjoining Idaho, a
rwo-'fold division of the Devonian is recognized. The
two units are roughly correlable with the Three Forks
and Jefferson of central'Montana. In the latter area,
a pre-JeffersOn basal clastic unit is also recognized and
the Jefferson Is divisible into an upper dolomite member and a lower limestone member. In sections I and
2 the lowest Devonian beds appear to be lithologic
equivalents of the dolomite member of the Jefferson,
and the lower limestone member is not lithologically
distinguishable. However, this limestone member becomes recognizable a short distance to the north. The
Three Forks Interval of southwestern Montana, is made
up of shale and argillaceous dolomite beds containing
a thin, varicolored, solution-brecciated zone' at the base.
Light-brown or orange-weathered, fine, sandy beds are
developed, in the upper, part of this clastic sequence,
directly below the Madison strata. These sandy beds
may be lithologic equivalents of the Sappington sandstone in the Logan -area of Montana, where they have
been included ih the Devonian by Sloss and Laird
(1947). Recently, Holland (1952) has assigned a
Kinderhookian age to the Sappington sandstone developed at Logan, Montana, and correlates the zone
with his Leatham formation of northeastern Utah mentioned above. The exact relationship of the Three Forks
beds with the Darby of western Wyoming requires
further study, but the upper part of the Darby appears
to be related to the Three Forks in that it also contains
prominent amounts of elastics. The Darby' typically
shows a shelf sequence msfde up predominantly of
secondary dolomites with variable amounts of normal
marine limestone. The sandstone has variable amounts
of carbonate cement and passes laterally into sandy
carbonates and pure carbonates. Green or gray clay
shales are also developed in thin beds or partings.
ISOPACH A N D FACIES MAP
isGpach Pattern
The isopach pattern (Figure 4) suggests the existence within the area of the map of two different tectonic
environments. Stable shelf conditions In the Wasatch
Range-—western Uinta Range area abd in the area of
west-central Wyoming and eastern Idaho are indicated
by the rather broad extent in both areas of relatively
thin Devonian sediments. The thickness of the Devonian section in these shelf areas averages between
150'and 300 feet. A gradual westward thickening from
the eastern zero edge is well portrayed, particularly in
the Wyoming Shelf (Andrichuk, 1951). The shelf
areas are bounded on the west by an irregularly trending axis of rapid increase in thickness. This zone presumably represents the tectonic "hinge" between the
shelf areas to the east and the more negative geosyn-
[J
30
F O U R T H
A N N U A L
FIELD
clinal areas to the west. The Wyoming Shelf is likewise bounded oh the north, off the area of the map,
by a west to east axis of rapid thickening trending
across southwestern Monaina.' Devonian sediments to
the north in Montana, increase to a thickness of about
C O N F E R E N C E
-
I 9 S 3
1,000 feet, while to the west and southwest of the Wyoming Shelf, in Idaho, and the northeastern edge of
Utah, thicknesses in excess of 3,0D0 feet are known.
The smaller shelf in north-central Utah is separated
from the Wyoming shelf by the geosyndinal embay-
if
I
.r
m
FIGURE 4.
ll
JEFFERSON
JEFFERSON
PM.
A
F M.
r
/
*THREE
1 ^
n N H n L fTM l-tJ N Ht-
"J E F F E R 5 O N
A
FOR K S ' FM.
SMIil
^FM
'^^^^m^^sm'mmmm^
eSJRDMSAi/
^£fJ8Eff
In
N T E R M O U N T A I N
A S S O C I A T I O N
ment in northeastern Utah. Thickening from the very
rhin sediments of the Utah shelf, to the geosyndinal
embayment to the north is moderarely rapid, with thicknesses of approximately 2,500 feet being attained. However, to the west of the Utah shelf thickening toward
the geosyncline is more gradual, and geosyndinal sediments in western Utah average about 1,500 feet.
Lithofacies Pattern
elastics are important constituents of the section
in both shelf areas mentioned above, and exhibit a
gradual decrease in proporrion westward from the zero
edge. Near the present eastern limit of Devonian occurrence, the elastics locally may be quantitatively more
important than the carbonates. In the shelf area of
Wyoming they generally constitute at least 20 per
cent of the total section. Non-elastics form over 80 per
cenr of the total section in the adjoining basinal areas
to the west and southwest. In 'Wyoming the elastics
become much coarser near the eastern zero edge. In
the Utah shelf, which is considerably narrower rhan
that in Wyoming, elastics near the eastern edge dominate the section, constituting at least 75 per cent of
the sediments present This condirion rapidly changes
to the west until in the exposures at the western edge
of the shelf in the Wasatch Range carbonates constitute the grearer part of the section.
TECTONIC A N D ENVIRONMENTAL
INTERPRETATION
The Utah and Wyoming shelf areas behaved as
relatively positive areas on which sedimentation commenced somewhat later than in the adjoining negative
areas to the west and north. Devonian clastic deposits
of the Utah shelf represent deposition under stable
conditions. The relatively fine sands and silts and clays
are of a clean character and suggest deposition under
conditions of stability with reworking of the depositional interface for considerable lengths of time before
lithification was completed. Carbonates at the western
edge of the Utah shelf likewise represent stable conditions, being of normal marine limestone type. Similarly,
to the northeast, in the Wyoming shelf area the elastics
and carbonates of the Darby represent shelf-type deposits laid down under relatively near-shore conditions
of considerable stability. Quartzose sands, showing
lateral intergradations with carbonates, green clay
shales, and well developed secondary dolomites all indicate slow deposition on a slowly subsiding platform,
permitting winnowing out of fine clastic material and
dolomitization of the limestones. The deposits are
characterized by evidences of disconformities, especially
in the eastern areas. The increasing clastic content and
OF
PETROLEUM
GEOLOGISTS
31
coarsening of elastics of the east indicate that the present
zero edge was also the approximate eastern deposirional
limit. The adjacent landmass to the east was apparently
sufficiently positive to furnish rhe coarse and fine elastics which are prominent at the sight of deposition.
The locus of rapid change in thickness bounding
the generally western edge of both the Wyoming and
Utah shelves represents a tectonic hinge which, consequently, also forms the eastern boundary of the irregularly trending geosyndinal belr. The fact that carbonate
sediments are predominant in this more negative belt
indicates that the belt lay a considerable distance from
the land area to the east from which the sediments of
the region were likely derived. Even in the area of the
southeastern Idaho embayment, which extends considerably closer to the sediment source area than do other
parts of the geosyndinal element, the section is composed predominanrly of non-clastic material, although
in this area elastics do become more noticeable in the
section (for example in the Logan, Utah area. Section
8, Figure 3 ) .
Pattetns shown in Idaho are constructed on the basis
of available published information (Mansfield, 1927,
Ross, 1934, 1937; Umpelby, 1913, 1917; Umpleby, et
al., 1930) and by use of unpublished material received
from L. L. Sloss and used by permission of Phillips
Petroleum Company.
BIBLIOGRAPHY
Andrichuk, J. M. ( 1 9 5 1 ) , "Regional Stratigraphic Analysis of Devonian System in Wyoming, Montana, Southern Saskatchewan, and
Alberta," Bull. Amer. Assoc. Petrol. Geol., Vol. 35, No. 11, pp.
2368-2408. •
Eardley, A. J. ( 1 9 4 4 ) , "Geology of the North-Central Wasatch Mountains, Utah", Bull. Geol. Soc. Am., Vol. 55, pp. 821-893.
Foster, H. L. ( 1 9 4 7 ) , "Stratigraphy of Teton County, Wyoming,"
Bull. Amer. Assoc. Petrol. Geol., Vol. 3 1 , No. 9.
Holland, Jr., F. D. ( 1 9 5 2 ) , "Stratigraphic Details of Lower Mississippian Rocks of Northeastern Utah and Southwestern Montana",
Bull. Amer. Assoc. Petrol. Geol., Vol. 36, No. 9, pp. 1697-1734.
Mansfield, G. R. ( 1 9 2 7 ) , "Geology, Geography, and Mineral Resources of Part of Southeast Idaho", U. S. Geo!. Survey Prof. Paper
152. p. 159.
Richardson, G. B. ( 1 9 4 1 ) , "Geology and Mineral Resources of the
Randolph Quadrangle, Utah, Wyoming", U. S. Geol. Survey
Bull. 923.
Ross, C. P. ( 1 9 3 4 ) , "Correlation and Interpretation of Paleozoic
Stratigraphy in South-Central Idaho", Bull. Geol. Soc. America,
Vol. 45, p. 937.
Ross, C. P. ( 1 9 3 7 ) , "Geology and Ore Deposits of Bayhorse Region,
Custer County, Idaho", U. S. Geol. Survey Bull. 877.
Sloss, L. L. and Laird, W. M. ( 1 9 4 7 ) , "Devonian System in Central
and Northwestern Montana," Bull. Amer. Assoc. Petrol. Geol.,
Vol. 31. No. 8, pp. 1404-30.
Sloss, L. L. and Moritz, C. A. ( 1 9 5 1 ) , "Paleozoic Stratigraphy of
Southwestern Montana". Ibid.. Vol. 35. pp. 2135-69.
Williams, J. S. ( 1 9 4 8 ) , "Geology of the Paleozoic Rocks, Logan
(Juadrangle, Utah", Bull. Geol. Soc. Am., Vol. 59, pp. 1121-1164.
Umpleby, J. B., Westgate, L. G. and Ross, C. P. ( 1 9 3 0 ) , "Geology
and Ore Deposits of Wood River Region, Idaho," U. S. Geol.
Survey Bull. 814.
Umpleby, U. B. ( 1 9 1 3 ) . "Geology and Ore Deposits of Lemhi
County, Idaho,'" Ibid., Bull. 528.
Umpleby, U. B. ( 1 9 1 7 ) , "Geology and Ore Deposits of the MacKay
Region, Idaho," Ibid., Prof. Paper 97.