Ill CONGRESO L A T I N O A K E R I C A N O D E P A L E O N T O L O G I A . M E X I C O .
S I M P O S I O SOBRE F L O R A S D E L T R I A S I C O T A R D I O , S U F I T O G E O G R A F I A Y P A L E O E C O L O G I A .
MEt!ORIA. p.67-81, 1 t a b . , 6 f i g . , 1 9 8 5 .
A SUMMARY OF THE BIOSTRATIGRAPHY OF THE NEWARK SUPERGROUP OF EASTERN
NORTH AMERICA
WITH COMMENTS ON EARLY MESOZOIC PROVINCIALITY
BRUCE CORNET
Superior Oil Company Geoscience Lab., 12401 Westheimer
Texas 77077 U.S.A.
Rd.
Houston,
PAUL E. OLSEN
Lamont-Doherty Geological Observatory,Columbia University, Palisades,
New York 10964 U.S.A.
ABSTRACT
The Newark Supergroup of Eastern North America consists of rocks
judged to range in age from early Middle Triassic through late Early
Jurassic. Dating is principally based on the recognition of seven palynological zones correlated with the European standard stages and on
correlation of vertebrates and megafossil plants. The basic floristic
trends are a decrease in diversity into the Early Jurassic and the rise
to strong dominance of the cheirolepidaceous conifers. Based on published radiometric scales, the Newark depositional episode lasted roughly
45 million years and was antecedent to the actual separation of the
North American and African Plates. Correlation of other Early Mesozoic
continental areas with the Newark allows the conclusions that there
was a shift from Late Triassic floral and faunal provinciality to
Early Jurassic homogeneity, and that this shift was synchronous with a
widening of the equatorial arid zone.
RESUMEN
El Supergrupo Newark, del Oriente de America del Norte, consiste
en rocas q u e a juicio de 10s autores tienen un margen de edad entre el
~ r i a s i c oMedio temprano y el Jurasico Temprano tardlo. La asignaci6n de
edad se basa principalmente en el reconocimiento de siete zonas palinologicas que se correlacionan con 10s pisos estandar europeos y en la
correlation mediante vertebrados y megafosiles vegetales. Las tendencias floristicas basicas son un decrement0 de la diversidad hacia el
Jurasico Temprano y el surgimiento a una dominancia fuerte de las coniferas del tipo Cheirolepidiaceae. De acuerdo con escalas radiom6tricas
publicadas, el episodic de deposit0 Newark dur6 unos 45 millones de
aiios y precedi6 la separaci6n de las placas de ~ m 6 r i c adel Norte y de
Africa. La correlaci6n de otras areas continentales del Mesozoico temprano con el Newark permite las conclusiones de qua en este lapso sucedi6 un cambio que a partir de la provincialidad de flora y fauna del
Triasico Tardio llev6 a la homogeneidad del Jurasico Temprano, y que
este cambio fue contemporsneo con el ensanchamiento de la zona arida
ecuatorial.
INTRODUCTION AND GEOLOGICAL CONTEXT
The Newark Su~erqroup(Figure 1) consists of a series of Early Mesozoic deposits
of principally red non-marine elastics and
minor thoeliitic igneous rocks exposed in a
long series of discrete basins from Nova
Scotia, C.anada to South Carolina, U.S.A.
(OLSEN, 1978; VAN HOUTEI'I, 1977; FROELICH and
OLSEH, 1984). The long axes of these basins
parallel the fabric of the Appalachian Orogene and in most cases the basin sequences
are preserved as internally faulted and tilted halfgrabens. A long series of closely related basins occur beneath the Atlantic Coastal Plain and on the Continental Shelf (OLSEM,
1978).
Most Newark Supergroup rocks were apbarently deposited in asymmetrically subsid-
68
CORNET
ing troughs formed along major Paleozoic
thrust faults,which were reactivated in the
Early Hesozoic as listric normal or normaloblique faults (LINDHOLM, 1978; PETERSON,
et al., 1984). There were at least several
kilometers of dip-slip movement during the
history of the basins. Whether these basins
formed in a simple extensional system acting
perpendicular to the axis of the basins or
in a wrench system acting oblique to the
fabric of the orogene is a matter of ongoing
&
OLSEN
debate (MANSPEIZER and OLSEN, 1981; MANSPEIZER, 1982); however, it is certain that these
basins formed just before
the onset of
actual separation of the North American and
African plates and the oldest formation of
Atlantic oceanic crust in the liiddle Jurassic (SUTTER and SMITH, 1979).
As much as 10 km of principally fluvial
and lacustrine sediments filled these basins.
Host sequences show a bulls-eye facies pat-
-
SCALE
Ikm I
0
.
.
.
800
.
.
.
.
.
A
EXPOSED
INFERRED
F i g u r e 1: T h e N e w a r k S u p e r g r o u p o f E a s t e r n N o r t h A m e r i c a . M o d i f i e d
f r o m OLSEN ( 1 9 7 8 ) . The i n f e r r e d a r e a s p r o b a b l y o v e r l a p
t h e N e w a r k i n a g e b u t some may n o t b e l i t h o l o g i c a l l y s i m i l a r t o t h e N e w a r k . Key t o F i g u r e i n T a b l e 1.
I11 CONGRESO LATINOAMERICANO DE PALEONTOLOGIA. FLORAS TRIASICAS
tern of coarse fluvial sediments alonq the
basin edges and finer sediments in the middle. Evidently most basins had internal
drainages and perched outlets and therefore
contained lakes as long as there was sufficient precipitation. Some of these lakes
covered more than 7,000 km2 and may have
been deeper than 100 in. In addition to fluviolacustrine sediments, several Newark Supergroup basins also contain extrusive basalt
sequences high in the sections, and in one
basin (the Fundy Basin in Nova Scotia, Cana-
~~~~0
da) there are a number of intervals of eolian
sandstone (HUBERT and MERTZ, 1980; OLSEN,
1981).
No marine fossils are known from the
Newark Supergroup and this has greatly hindered correlation of these continental beds
with the standard European section. Fortunately most intervals contain at least some
beds with well preserved pollen and spore
assemblages, megafossil plants, and terrestrial and aquatic vertebrates. These allow
an internal correlation of the Newark as well
B a s i n name
~ o c k - s t r a t i g r a p h i cterm
Age r a n g e
I
1
1
Chatham Group
1
Deep R i v e r B a s i n
1
Carnian-?Norian
(Late T r i a s s i c )
1
2
1
undifferentiated
1
Davie County B a s i n
1
?Late T r i a s s i c
A
1
1
5
undifferentiated
Farmville Basin
?Carnian ( L a t e
Triassic)
undifferentiated
4 small basins south
o f F a r m v i l l e Basin
Â¥!Carnia ( L a t e
Triassic)
Dan R i v e r Group
1
Lkn R i v e r a n d D a n v i l l e
Bas I n s
1
Carnian-?Norian
(Late T r i a s s i c )
6
Tuckahoe and
C h e s t e r f i e l d Groups
Richmond B a s i n a n d
subsidiary basins
Carnian (Late
Trjaç8ic
7
C u l p e p e r Group
Culpeper Basin
Norian-~Sinemurian
(Late TriassicEarly Jurassic)
4
T a y l o r s v i l l e Basin
1
1
9
I
undifferentiated
I
S c o t t s v i l l e Basin and
2 subsidiary basfns
I
1
Carnian (Late
Triassic)
?Late T r i a s s i c Early Jurassic
10
none
Gettysburg Baain
Carnian-Hettangian
(Late TriassicEarly Jurassic)
11
none
Newark B a s i n
Carnian Sinemurian
(Late T r i a s s i c Early Jurassic)
none
Pomperaug B a s i n
?Late T r i a e s i c Early J u r a s s i c
13
none
H a r t f o r d Basin and
s u b s i d i a r y Cherry
Brook B a s i n
Nor inn-?Be j o c i a n
(Late T r i ~ i ~ i c ?Middle J u r a s s i c )
Ill
none
D r e r f i e l d Basin
7Norian-?Toarctan
(Late T r i a s s i c Early Jurassic)
15
Fundy Croup
Funily Baa i n
?Middle T r i a s s i c Early J u r a s s i c
16
Chedabucto F o r m a t i o n
(-Eurydice Formation?)
Chedabucto Basin
(-Orpheus B a s i n ? )
?Late T r i a s s i c Early Jurassic
12
1
6
I
59
T a b l e 1: D i v i s i o n s o f t h e N e w a r k S u p e r g r o u p a n d k e y t o F i g u r e 1.
Note t h a t "none" under t h e r o c k - s t r a t i g r a p h i c t e r m categor y i n d i c a t e s t h a t , a l t h o u g h t h e r o c k s o f t h e b a s i n may
h a v e b e e n d i v i d e d i n t o f o r m a t i o n s , n o i n c l u s i v e name f o r
a l l t h e f o r m a t i o n s o f t h a t b a s i n have been proposed. Modif i e d f r o m OLSEN (1978).
CORNET
70
as correlation with the European standard
stages and other Early Mesozoic sections.
We address 4 main goals in this paper:
1) to summarize theage-correlativedata from
the Newark, concentrating on the pollen and
spore and vertebrate assemblages; 2 ) to relate this local chronostratigraphic framework to other continental Early Mesozoic
areas and the European standard stages; 3)
to attempt to calibrate the biostratigraphy
of the Newark by correlation with published
radiometric scales; and 4) to use information
from these correlatiorsto briefly examine
floral and faunal provinciality during the
Early Mesozoic.
&
OLSEN
PALYNOLOGICAL CORRELATIONS
Plants, especially pollen and spores,
are of paramount importance to the biostratigraphy of the Newark. CORNET (1977a) proposed seven pollen and spore zones,which are
summarized below and in Figures 2 and 3. The
oldest zone, the Chatham-Richmond-Taylorsville palynoflora, is recognized in the
Chatham Group of the Deep River Basin and in
the Richmond and Taylorsville basins, and
contains about 155 pollen and spore species.
This assemblage can be divided into two
subzones.
European
Standard
tages
TOARCIAN
LIENSBACHIAf
NORIAN
CARNIAN
LADINIAN
ANISIAN
Figure 2:
I n t e r n a l c o r r e l a t i o n o f t h e Newark, based on f a u n a l and
f l o r a l d a t a ( c o r r e l a t i o n s b a s e d o n d a t a p r e s e n t e d i n CORNET
( 1 9 7 7 a , 1 9 7 7 b ) , ULSEN a n d GALTON ( 1 9 7 7 , i n p r e s s ) , OLSEN,
McCUNE a n d THOMSON ( 1 9 8 2 ) a n d OLSEN ( 1 9 8 3 a , 1 9 8 3 b ) .
W i t h i n each column r e p r e s e n t i n g a s i n g l e b a s i n , t h e
d a r k g r a y zones r e p r e s e n t p r i n c i p a l l y l a c u s t r i n e r o c k s
w h i c h a r e d o m i n a n t l y g r a y o r b l a c k ; t h e l i g h t e r g r a y zones
represent l a c u s t r i n e rocks which are dominantly red b u t
w h i c h may h a v e s i g n i f i c a n t g r a y b e d s ; t h e w h i t e z o n e s a r e
d o m i n a n t l y f l u v i a l o r unknown; t h e v e r t i c a l l y r u l e d zones
r e p r e s e n t e x t r u s i v e b a s a l t f o r m a t i o n s w h i c h o f t e n have i n terbedded s e d i m e n t a r y f o r m a t i o n s w i t h l a c u s t r i n e r o c k s ; and
t h e zone marked w i t h " x " s r e p r e s e n t s a l t d e p o s i t s i n t h e
o f f s h o r e Orpheus Graben. H o r i z o n t a l l i n e s w i t h i n t h e columns a r e forma t i o n b o u n d a r i e s .
190
MA
EUROPEAN
STANDARD
STAGES
-
COROLLINA
TOARCIAN
MURPHY1
COROLLINA
200
--
PLIENSBACHIAI
TOROSUS
SINEMURIAN
208
-
----
COROLLINA
MEYERIANA
HETTANGIAN
.
MANASSASUPPER
PASSAIC
NORIAN
LOWER
PASSAIC-
220
230
HEIDLERSBURO
-
-
LATE
NEW OXFORD-
CARNIAN
LOCKATONG
MIDDLE
CARNIAN
RICHMONOTAYLORSVILLE
F i g u r e 3 : The d i s t r i b u t i o n o f a g e - d i a g n o s t i c p a l y n o m o r p h t a x a w i t h i n
t h e Newark S u p e r g r o u p ( d a t a a d a p t e d f r o m C O R N E T , 1 9 7 7 a ) .
CORNET
A lower subzone is dominated either
by crywtoqam spores and gymnospermous
monosulcate pollen, or by a diversified
gymnospermous assemblageof non-striate bisaccate and circumsaccate pollen with minor
percentages of monosulcate pollen, circumpolles, tetradopolles, and striate bisaccate
pollen. This subzone occurs in the Richmond
and Taylorsville basins. A similar pollendominated assemblage occurs in the basal
Pekin Subbasin of the Chatham Group. A i a t / i i b p o i i t e b b c a b > i a t u b , A. 6 i m b i i a t u b , CaLamobpo i a n a t h o h b t i i i L , and La.>n.coidiiteb spp. make up
the dominant cryptogram elements of the oldest spore and monosulcate-dominated assemblage, while O b m u n d a c i d i t e - i i spp. , 8 a c u t a t i . h ? ~ V i i t e bspp., and G'io.nu.tat-i&po/iiteb
spp.
compete with articulate spores (e.g. L a i i c o i d i t e b sv. and P i t a b o o i i i t e b sp.) for dominance
in younger spore-dominated assemblages.
These contrasting cryptogamous and
gymnospermous palynofloras alternate with one
anotherthrough the Richmond-Taylorsville basin
sequences as the lithologic facies alternate
from deltaic-lacustrine to fluvio-deltaic.
Based on recent well data from the Richmond
Basin, at least two upwards-coarseninglacustrine to fluvial sequences, and the "head
and tail" portions of two additional sequences record the cyclic waxing and waning
of a large rift valley lake.
The upper subzone contains a less diversified spore assemblage and has more abundant
P a i i n c i t i p v t - i t i l i d e n b u b , a circumsaccate morphotype that ranges down to the oldest Richmond Basin strata. The upper subzone also
lacks A i a t i - i & p o i i t e t , spp. and contains only
rare striate bisaccate pollen, which decrease
in abundance and diversity upwardsthrough
the lower subzone. This upper sub-assemblaoe
occurs in the upper Pekin Formation and
Cumnock Formations of the Chatham Group, the
lower New Oxford Formation of the Gettysburg
Basin, and perhaps the lower Wolfville Formation of the Fundy Group (TRAVERSE, 1983).
Age-diagnostic species of the oldest
zone include the overlapping ranges of P a t i nabpoi'itei denbui, Stiiatoab'ie-ite.h a g X u g i i ,
Th-t.adibpo/ic( v e i ' i u c a . t . a , P t o X o d i p L o x y p i n u b
doubA.nge.'ii, Pfica-fccAaccub b a d - i u b , T ~ L a d i b p o t a
cf T . a u t e c ~ , and L a g e n e t e a m a n . t i n i i , indicat-
.
ing a orohable late Middle Carnian age. However, palynoflorules older than Middle Carnian are only now becoming well known in
Europe and it is possible that the beds of
the Richmond and Taylorsville basin may be
substantially older than this assessment perhaps even as old as Middle Triassic.
The upper sub-assemblage of the ChathamRichmond-Taylorsville palynoflora is replaced upwards in the Gettysburg Basin by the
New Oxford-Lockatong palynoflora, which has
also been recognized in the Newark
(CORNET, 1977a) and Dan River basins (ROBBINS, 1982). This assemblage is dominated
by P a t i n a b p o n . H e . i i d e n b u b , V a t t i b p o h - i t a ig n a c i i , A t i b p o h - i t e b p a i v u b , and T i i a d i i b p o i a
spp. It still contains C a m e i o b p o i i t e b b e c a t u b and C. p b e u d o v e ~ i u c a t u ~but
,
lacks the
Middle Carnian age-diagnostic taxa of the
&
OLSEN
Chatham-Richmond-Taylorsville 'palynoflora,
all of which indicate that it is of Late
Carnian Age.
The New Oxford-Lockatong palynoflora
is gradually replaced upwards in the Newark
Basin by the Lower Passaic-Heidlersburg
palynoflora found thus far in the Culpeper,
Gettysburg, Newark, and Hartford basins.
This assemblage is distinguished by the presence of C a m e i o b p o i i t e t , u e i i u c o b u b , an abundance of large and varied bisaccate species,
including the giant A i i h p o f i ^ t u o p - i L , and
the continued dominance of P a t i n a ~ p o h i t e i
d e n h u b , V a H a b p o & ^ t s . f i i g n a c i i , and T i i a d i b p o i a spp. This assemblage appears to be of
Norian age. The upper portion of this zone,
in the Newark Basin, contains the first
rare occurrences of C o i o t t ^ n a m e y e i i a n a .
The Lower Passaic-Heidlersburg palynoflora slowly changes upwardsinto the Manassas-Upper Passaic palynoflora in the Culpeper and Newark basins. This zone is distinguished by the first occurrence of C o i o U h a
t o i o b u b and G i a n u t o p e ~ t c u t a t  ¥ ( . p o t imi d i b and
the continuation of taxa common in the previous zone. This zone correlates with what
palynostratigraphers have been calling the
Rhaetian in Europe. The Rhaetian was first
defined in marine rocks in the Austrian Alps,
but these rocks have been recently shown to
be partly equivalent to marine Late Norian
strata elsewhere in Europe (PEARSON, 1970;
TOZER, 1979). A number of authors do no
longer consider the Rhaetian to represent an
independent stage. What its loss does to the
palynologically defined Rhaetian is unclear.
However, Rhaetian palynofloras probably
should be regarded as Late tlorian, while
'typical" Norian assemblages are probably
best regarded as Early and Middle Norian.
The Manassas-Upper Passaic palynoflora is
thus Late Norian in age and is recognized in
the Culpeper, Newark, and possibly Fundy
basins (The name Manassas was originally
chosen for palynoloqical localities near
Manassas, Virginia, and does not refer to
the Manassas Formation of the Culpeper
Basin, which is older).
This latter zone ends upwards with a
rapid transition to the C o - t o H i n a meyet^.ana
palynoflora, which is characterized by a
switch from a high diversity assemblage dominated by bisaccate pollen, Pat-Lnab , p c i - i t e b ,
C o i o i i i n a m e y i t i a n a , C . t ~ t ~ b and
~ b G, t a n u tope.'icuLat-iiJo/t'i^
i u d i b to a low diversity
assemblage very strongly dominated (+go%)
by the circumpolles C o t o t i i n a m e y e i i a n a .
This transition takes place over an 80 m
thick "barren" interval below the Orange
Mountain Basalt in the Newark Basin (Jacksonwald Syncline). By the top of this interval, all taxa characteristic of the Late
Triassic are absent. The high diversity
assemblage below this interval is peculiar
in having a suite of pollen grains showing
all the characters typical of angiosperms,
although they are not assignable to any
known angiosperm group. According to DOYLE
(1978), "...these grains are perhaos the
best candidates yet for pre-Cretaceous
I11 CONGRESO LATINOAMERICANO DE PALEONTOLOGIA. FLORAS TRIASICAS
73
Above the Zone of E o g i n k g o i X e . ~is ASH'S
Zone of V i n o p h y t o n , a conifer-like gymnosperm.
This zone has been recognized in the upper
member of the Cow Branch Formation of the Dan
The C o i o f i i n a meq&ana
palynoflora is
River Basin (OLSEN it a t . , 1978), and in the
characterized by the first common appearance
middle New Oxford Formation of the Gettysburg
of C c i : i ! o f u t 4 . 5 p o i a htuk^fio^.ma; this zone is the
Basin (ASH, 1980; WARD, 1900; CORNET, 1977b).
lowest of the Jurassic pollen and spore zones
Newark assemblages from this zone are somein the Newark. The Triassic-Jurassic boundary
times dominated by conifers,but are generally
is best ?laced just below the Orange Mountain
still diverse with an abundance of bennettitaBasalt and the oldest extrusives in other
leans. These florules are still poorly known.
basins (CORNET, 1977a, 1977b) rather than withThe youngest zone recognized by ASH is
in the zone of extrusives as suggested by
called simply the Upper Zone. This zone is
CORNET, et al. (1973) and CORNET and TRAVERSE
strongly dominated by cheirolepidaceous coni(1975). "BIG C o i o i t i u a me.yeh-ia.na palynoflora confers, especially B k a c h y p h y t t u m , Pagio'phqSLtum,
tinues through the entire zone of extrusives
and Uiime.te.LLa. The cycadeoid OtozanlUe.5 anJ the
and into the overlyinq sediments in all of the
fern Cta.tl~,toptn'i.'iii are often common. Compared
Newark Supergroup Basins. Pollen and spore
to the older two zones, the florules of this
assemblages do not allow a finer subdivision
zone are of very low diversity. This zone is
within this zone or a correlation of individurepresented in the syn- and post-extrusive
al sedimentary formations between extrusives
sediments of the Culpeper, Gettysburg, Newark,
in different basins. This zone seems to cover
Pomperaug, Hartford, and Deerfield basins.
all of the Hettangian and Sinemurian of the
Scattered descriptions of elements of these
Early Jurassic.
florules were described by EMMONS (1857).
The C o i c i f f i n a ¥('0^.0.5upalynoflora succeeds BOCK (1969), and especially NEWBERRY (1888),
the i.'. i n e y c i i a n a palynoflora upwards with a
and CORNET (1977a), but these are diverse
strong switch in the dominant taxon from C o i o assemblages which definitely can be further
Pf-ciia mcye..iiana to C . XokoAu.5. This switch ocsubdivided.
curs in the beds some distance above the upperThe Zone of E o g - i i i k g o i t e . ~ corresponds
most extrusives in the Culpeper and Hartford
broadly to CORNET'S (1977a) Chatham-Richmondbasins. The age of this assemblage appears to
Taylorsville palynoflora and it is thus Middle
be Pliensbachian.
Carnian (or older) in age. The Zone of 'D-in.0In the Portland Formation of the Hartford
,3hyton corresponds to the New Oxford-Lockatonq
Basin there is one zone younger than the C o k o palynoflora and is Late Carnian in age. The
€£<-i
t f a o 5ub palynoflora. The C o i o f t i n a mu^.Upper Zone corresponds to the Jurassic pollen
. ,. salynoflora occurs in the highest sampled
,
and spore zones of CORNET (1977a). It should
horizons in the Portland and, hence, in the
also be noted that this last assemblage clearNewark Supergroup. It is characterized by a
ly resembles what is called the H.iime.ie.tta
dominance of Co?cCC4iti! mu4p11y4 over C . .('Oi0.5ub
( C d e L t o t t p i ~ )assemblage, typical of the Early
(52% vs. 39% . The age of this assemblage a?Jurassic of Great Britain (CORNET , 1977a)
pears to be Toarcian.
and it probably corresponds to Harris's
Zone of T h a u m a . t o p . t e . i i ~ (ASH, 1980) of Hettangian age. ASH based his zones mostly on
RELATIONSHIP OF PALYNOMORPH ZONES
deposits in the Western United States. There
TO MEGAFOSSIL ZONES
is as yet no definitive evidence for sediments intermediate in age between the Late
Although the megafossil ~ l a n t sof the
Carnian and the Early Jurassic in that area.
Newark were a major focus of research, parTherefore, ASH did not recognize megafossil
ticularly with regard to age, in the late
plant zones that might correspond to the
19th and early 20th centuries, much less
Lower Passaic-Heidlersburq palynoflora or
attention has been paid to them since the
the Manassas-Upper Passaie palynoflora in
1920's. Recently, ASH (1980) has reviewed
the Newark. NEWBERRY (1888), BOCK (1969, in
North American Early Mesozoic plant assempart) and CORNET (1977a) have described some
blages and divided them into three zones all
florules corresponding to these palynomorph
of which are represented in the Newark Superzones, notably that of Milford, New Jersey
qroup (Figure 3).
from beds of the Lower Passaic-Heidlersburg
palynoflora. In any case, the megafossil
The oldest is called by ASH the Zone of
assemblaqes from these latter two zones of
Eog-inkjoi.te.fi, a bennettitalean gymnosperm.
the Newark are the least well known of the
The zone of which it is typical has been
supergroup.
identified in the Newark in the Richmond Basin, the Pekin, and the Cumnock Formations
In very broad terms, the most obvious
of the Deep River Basin, and the Stockton
floral trend visible through the entire
Formation of the Newark Basin (ASH, 1980).
Newark section is decreasing floral diversity.
Florules of this zone are the most diverse
The oldest beds of the Newark, typified by
in the Newark Supergroup, with very common
the Richmond Basin section, have both the
ferns and bennettitaleans. Florules in this
largest number of described megafossil spezone include those described by FONTAINE
cies and the largest number of pollen and
(1883), HOPE and PATTERSON (1970), DELEVORYAS
spore morphotypes. As important as the number
and HOPE (1971, 1975, 1976). EMHOMS (1856.
of taxa is, no single taxon is consistent1857), WILLARD et al. (1959), BROWN (1911),
ly dominant from locality to locality within
and BOCK (1952, 1969, in part).
the Richmond Basin and at some localities the
angiosperms...". An assemblage of somewhat
similar grains occurs in the Chatham-Richmond-Taylorsville palynoflora.
.!?
,
-
-.,
w
7
8
$
DICTYOPYGE SPP.
TANAOCROSSUS SP.
CIONICHTHYS SPP.
SYNORICHTK~SSP.
"DIPLURUS" (PARIOSTEGEOUS) SP.
"DIPLURUS" (OSTEOPLEURUS) SP.
TURSEODUS SPP.
"PHOLIDOPHORID"
CARINACANTHUS JEPSENI
"SEMIONOTUS BRAUNII GROUP"
SEMIONOTUS SPP.
CF. HYBODUS SP.
PTYCHOLEPIS SPP.
REDFIELDIUS SP.
ISCHYPTERUS SPP.
"SEMIONOTUS ELEGANS GROUP"
DIPLURUS LONGICAUDATUS
"ACENTROPHORUS" CHICOPENSIS
"TREMATOSAUR"
CF. APHANERAMA SP.
CF. ANOMIODON SP.
CF. SCLEROSAURUS SP.
CF. EXAERETODON SP.
CF. PROTOROSAURUS SP.
TANYSTROPHEUS SP.
"TRILOPHOSAURS"
"RAUISUCHIDS"
"DICYNODONTS"
DOSWELLIA KALENBACHI
~ICTYOCEPHALUSELEGANS
TENUIROSTRIS
" MICROCONODON
-. DROMETHERIUM SYLVESTRE
(T "CAPITOSAURS" (INCL. CALAMOPS)
(rt
"TYPOTHORAX" SP.
METOPOSAURUS (INCL. EWELOR) SPP.
CÃ SCALENODONTOIDES SP.
LEPTOPLEURON SP.
"3 NEW PROCOLOPHONIDS"
PARADAPEDON
ICAROSAURUS SEIFKERI
2. STAGONOLEPIS
AETOSAURUS
TAOTTRACHELOS SPP.
--
"THECODONTOSAURUS" GIBBIDENS
STECOMUS SPP.
SFHODROSAURUS PENNSYLVANICUS
AFF. SPHENODON SP.
RUTIODON SPP.
"PHYTOSAURS" (INCL. CLEPSYSAURUS)
HYPSOGNATHUS FENNERI
"SMALL SAURISCHIANS"
AFF. GLEVOSAURUS SP.
"FABROSAURID"
STEGOMUSUCHUS SPP.
AMNOSAURUS SPP.
ANCHISAURUS SOLUS
PODOKOSAURUS HOLYOKENSIS
5
01
TRIASSIC
JURASSIC
BRACHYCHIROTHERIUM SPP.
APATOPUS SPP.
GWYNEDDICHNUS SPP.
"ANCHISAURIPUS" MILFORDENSIS (N.GEN. l
RHYNCIIOSAUROIDES HYPERBATES
RHYNCHOSALROIDES BRUKSWICKII
BRACHYCHIROTHERIUM EYERMAUI
BRACHYCHIROTIIERIUM PARVUM
GRALLATOR (GRALUTOR) SPP.
RHYNCHOSAUROIDES SPP.
GRALLATOR (ANCHISAURIPUS) SPP
GRALLATOR (EUBRONTES) SPP.
BATRACHOPUS SPP.
OTOZOUM SPP.
ANOMEOPUS SPP.
AMEGHINICIINUS SF.
I11 CONGRESO LATINOAMERICANO DE PALEONTOLOGIA. FLORAS TRIASICAS
relative abundances of taxa are surprisingly
evenly distributed. By the Late Carnian,
however, conifers often dominate the macroflora, and conifer pollen is dominant in the
microflora. The dominance of one taxon in the
microflora rarely exceeds 50%. In the Early
Jurassic Newark, however, conifers are very
strongly dominant in both macro and microfloras and often comprise more than 90% of the
assemblages.
VERTEBRATE ZONES
Vertebrate fossils are relatively common
in most parts of the Newark Supergroup, especially fishes and reptile footprints. OLSEN,
McCUNE, and THOMSON (1982) and OLSEN and
GALTON (1977; 1984) have reviewed much of the
biostratigraphically useful vertebrate data
and recognized a number of informal biostratigraohic zones. Recent discoveries have shown
that the useful biostratigraphic zones are
fewer in number and less complex than originally thought(OLSEN, 1983a, 1983b). The distribution of vertebrates in the Newark and
the zones they define are shown in Figure 4.
Note the correspondence between the upper
limit of the A p a - t o p u ~ zone and the base of
the C o t o . U i n a me.qe.n.-iana palynoflora and the
apparent lack of correspondence of the boundaries of the other vertebrate zones with the
palynoflora zones.
The oldest Newark vertebrate assemblage
occurs in a small isolated deposit within the
Fundy Basin (A of Figure 4). Vertebrates from
this deposit differ from all others in the
Newark and indicate an early Middle Triassic
(Anisian) age for the deposit. These are the
oldest beds in the Newark. No floral data
are available from these beds, unfortunately.
The next oldest assemblage occurs in the
Richmond, Taylorsville, and Scottsville basins (B of Figure 4) and is characterized by
vertebrates found nowhere else. Typical is
the-unique refieldiid fish V i c t y o p y g e . This
assemblage characterizes the lower part of
the Chatham-Richmond-Taylorsville palynoflora zone and appears to be of Middle Carnian
age, but it might be older.
The abundance of phytosaur reptiles
makes up the next assemblage (C of Figure 4).
which is characteristic of Late Triassic
vertebrate assemblages from other parts of
the world such as the German Middle and Late
Keuper. The upper Chatham-Richmond-Taylorsville through the Lower Passaic-Heidlersburg.
palynofloras contain this phytosaur-dominated
a~semblaqe~which
makes up the bulk of the
Newark.
The youngest Newark vertebrate assemblage
is characterized by a dominance of the remains
of dinosaurs and crocodiles and has no counterpart in the European Late Triassic (OLSEN
and GALTON, 1977, In Press) (D and E of Figure 4). Correspondingly the associated palynofloras are the Col.oi!t^.nn. m e y e k i a n a . through
the C o - t o ~ ~ i nmufipk-i'i
a
palynofloras, themselves
correlated with the Early Jurassic. This as-
semblage has its oldest representatives in
the sediments above the oldest extrusives in
the Newark.
CALIBRATION OF THE NEWARK
Five current and somewhat different radiometric scales are available for the Early
Hesozoic on a stage by stage level (Figure 5).
~ l five
l
scales use partially independent
data and have rather different age assignments
for the boundaries between stages and periods
(Figure 5). The lengths of the intervals
between stages are. however, closely comparable. These scales can be tied to the Newark
using the palynologically defined age-boundaries, discussed above. Within the Newark the
best defined boundaries are the Middle Carnian
Late Carnian boundary, the Norian Hettanqian boundary and the Pliensbachian Toarcian boundary. To apply the radiometric
scales to the Newark we have had to assume
that the Late Carnian was 1/3 the duration of
the Carnian and, of course, assume that the
correlation of the radiometric scales with
the European standard stages are correct.
The duration of intervals within most of
the Newark calibrated by the available radiometric scales are in very good agreement with
independent calibration by lacustrine sedimentary cycles ascribed to climate control by
the 21,000 year precession cycle (VAN HOUTEN,
1969, 1980; OLSEN, 1984af 1984b). However,
the thicknesses of the palynologically defined Middle Carnian of the Newark is out of
proportion with the 1.5 - 3.5 million years
alloted to the Middle Carnian in the published scales. If the sedimentation rates ascribed to the palynologically defined post-Middie Carnian of the Newark were similar to
those of the Newark Middle Carnian, the duration of the pre-Late Carnian of the Newark
would be on the order of 10 million years.
This suggests either a major problem with
assessments of the duration of the Carnian,
problems with correlation of the palynoflorules of the Newark with the European
section, or the possibility that the sedimentation rates for the older beds were
significantly higher. The last possibility
is in line with sedimentological data from
the Richmond Basin.
-
CORRELATION WITH OTHER AREAS OF CONTINENTAL
'SEDIMENTATION
Important areas of early Mesozoic continental sedimentation outside the Newark
include the European Keuper and Infralias,
the Newark Supergroup-like basins of Morocco,
the Chinle Formation, Dockum Group, and Glen
Canyon Group of the southwestern United
States, the Stormberg Group of southern Africa, the Ischiqualasto and Los Colorados of
Argentina, and finally the Lower Lufeng of
China. Correlation between some of these
areas and the European standard stages is
hampered by a lack of some classes of age-
RADIOMETRIC SCALES
Newark Supergroup
0,
CD
:
CV
m
0)
-
6
"
2
0
-1
-
Southwest
-
< g 0 )
s
0)
g
187
0
-I
<
VERTEBRATE
EUROPEAN
PALYNOFLORA
ZONES
STANDARD
STAGES
ZONES
-
182
T
T
188
194
~
~
~
~
TOARCIAN
-
P
u. s.
'
L
ZONES
(ASH, 1980)
/
-T
197
7
RAKENSBURG
-
GLEN
TOROSUS
s
s
206
s
204
SINEMURIAN
205
208
----
H
Ti200
I
GROUP
CLARENS
UPPER
MEYERIANA
UPPER
213
UPPER
N
N
LOWER
PASSAICHEIOLERSBIWG
225
225
LC
LC
M-E
C
M-E
230
230
c
218
225
LC
LC
M-E
-,
LATE
NEW OXFORD
CARNIAN
LOCKATONQ
!
CHINLE
DINOpHyTON
-
MIODLE
c
CARNIAN
-
ELLIOT
. - - - -
L
L
235
A
A
240
240
W
AD
L
A
ANISIAN
235
MOENKOPI
238
A
-- -
COLORADOS
ELLIOT
LOW
LOW
LUF
x
MOLTEN0
LOWER L O S
COLORADOS
ISCHIGUALASTO
FAYLORSVILLE
L
LUF
-7-
UPPER L O S
LOWER
232
235
UPP
LOW
M-C
DOCKUM
U-E
7
/'
COROLLINA
HETTANQIAN
-
f
CANYON
MANASSAS-
N
Ch
VOLCANICS
-
-
Yun
COROLLINA
MURPHII
200
198
U
~
P
P
208
E
184
T
193
M
Ourita
Karoo
Basin
Basin Argentina
Morocco S. Africa
BEAUFORT
I11 COMGRESO LATINOAMERICANO D E PALEONTOLOGIA. FLORAS TRIASICAS
correlative data, such as palynomorphs or
marine invertebrates, but correlation by vertebrates through the Newark provides the necessary and crucial link. Figure 5 shows an
attempted correlation of the above areas with
the Newark and the European standard stages.
Of particular interest are the assignments of the entire Glen Canyon Group of the
southwestern United States, the Upper Stormberg Group, and the upper Lower Lufeng of
China to the Early Jurassic (OLSEN and GALTON,
1977, In Press). Until recently, the prevailing view was that all these intervals were
Late Triassic in age. With these new age designations in mind, we can look at the pattern of "climate sensitive" rocks and floral
and faunal provinciality for the Late Triassic and Early Jurassic (Figure 6).
LATE TRIASSIC PROVINCIALITY
Prominent in the pattern of deposits of
Late Triassic Age is a zone between north 40
and south 30 paleolatitude where phytosaur
reptiles and metoposaur amphibians are common
(the latter only in the Carnian) (Figure 6).
They are present even in northern Gondwanaland (Morocco and India) but are absent in
the rich continental assemblages of the Ischiqualasto and related formations of South America and the Molteno and Lower Elliot formations
of Africa. This equatorial assemblage is dominated by archosaurs whereas the more southern contemporaneous assemblages are dominated by mammal-like reptiles.
The metoposaur-phytosaur biogeographic
province has floral counterparts. In the
Late Triassic, all vertebrate assemblages
south of 30 paleolatitude are associated with
0-tcto-t.d-t.um-type
megafossil florules. Only in
India do phytosaurs and metoposaurs occur
with a P-tcto-tdkum-typeflorule. In all other
areas, phytosaurs and metoposaurs occur with
a typical Laurasian bennetitalean-conifer
assemblage. The areas which have U-tc~oidiumtype florules are dominated by palynoflorules
of the Ipswich-Onslow-type (DOLBY and BALME,
1976; TRUSWELL, 1980), including India (KUMA-
RAN and HAHESWARI, 1980). In the northern
hemisphere, phytosaurs and metoposaurs are
absent above 30 north; however, there does
not seem to be a separate northern floral
province in the region where these vertebrates are absent.
Coals are fairly common in Late Triassic rocks north of 30 north and south of 30
south latitude (ANDERSON and ANDERSON, 1970;
ROBINSON, 1971, 1973). In between are scattered occurrences of evaporites and dune
sands and much less common coals (Figure 6).
Between north and south 30; the coals seem
to be restricted toanequatorial belt, but
there are so few occurrences, the pattern
may not be meaningful. It is worth noting,
however, that an arid-to-the-north trend has
been noted within the Newark Supergroup which
does conform to this postulated pattern
(HUBERT and MERTZ, 1980; OLSEN, 1981; MANSPEIZER, 1982).
EARLY JURASSIC PROVICIALITY
In contrast to the Late Triassic, no
continental vertebrate provinciality is visible in sediments of Early Jurassic age
(Figure 6). This faunal homogenization extends
to the intercontinental distribution of many
terrestrial vertebrate genera, especially
dinosaurs and mammals (OLSEN and GALTON, In
Press). This lack of provinciality also seems
to correspond to a reduction in the rate of
turnover for faunal assemblages as a whole. A
parallel pattern is apparent in Early Jurassic plants.
It has long been recognized that the
strong floral provinciality which characterized the Late Triassic world gave way in the
Early Jurassic to a more hcirogeneous world flora
dominated in nany areas by cheirolepidaceous
conifers (ALVIN, 1982); this dominance is
especially obvious in the preponderance of
C o n o U w a (Cta.i.iopo.C.C-tb)
pollen in many areas.
HUGHES (1973) has shown that in the Late Jurassic, the relative abundance of Coho!H.ina
was greatest in the equatorial region, and it
seems clear that this pattern was establish-
F i g u r e 5 : ' C a l i b r a t i o n o f t h e Newark b y p u b l i s h e d r a d i o m e t r i c s c a l e s
and c o r r e l a t i o n o f t h e b i o s t r a t i q r a p h i c s u b d i v i s i o n s o f
t h e Newark S u p e r g r o u p w i t h o t h e r E a r l y M e s o z o i c c o n t i n e n t a l
d e p o s i t s . S o u r c e o f d a t a f o r t h e s e c o r r e l a t i o n s same as
F i g u r e 4 a n d i n a d d i t i o n , MANSPEIZER ( 1 9 8 2 ) .
A b b r e v i a t i o n s a s f o l l o w s : R a d i o m e t r i c s c a l e s : A, A n i s i a n ; L , L a d i n i a n ; M-E C , M i d d l e a n d E a r l y C a r n i a n ; L C,
L a t e C a r n i a n ; N, N o r i a n ; H, H e t t a n g i a n ; S, S i n e m u r i a n ; P ?
P l i e n s b a c h i a n ; T, T o a r c i a n . V e r t e b r a t e Z o n e s : A - E, d e s i g nations o f v e r t e b r a t e asseblages discussed i n t e x t . O u r i t a
B a s i n : AD, a d e n s i t e ; M-C, M i n u t o ~ a c c u ~ - P a t ^ . n a ^ p o ' i H e ~
a s s e m b l a g e ; T , t h o l e i i t j c e x t r u s i v e b a s a l t s ; JC, J u r a s s i c
m a r i n e and p a r a l i c c a r b o n a t e s .
Note t h a t i n t h i s Figure the radiometric scales a r e
a l l t i e d a t the Pliensbachian-Toarcian, Norian-Hettangian,
and M i d d l e C a r n i a n - L a t e C a r n i a n b o u n d a r i e s as p a l y n o l o g i c a l l y f i x e d i n t h e Newark.
CORNET
I
G
Figure
OLSEN
6
I11 CONGRESO LATINOAMERICANO DE PALEONTOLOGIA. FLORAS TRIASICAS
ed by the Early Jurassic. Going from south
to north, there is a trend from C o ~ o H i n a dominated (+go%) to CoaoH-ivta-poor(-10%) microflorules (PEDERSON and LUND, 1980) with
transitional assemblages occurring around a
25 north ,-ialeolatitude. This pattern is reflected in the megafossils as well, with
conifers strongly dominant in the equatorial
region and much less so in the north. Data
are as yet insufficient to recognize a similar trend in the southern hemisphere.
Coals are virtually restricted to the
high latitudes in the Early Jurassic (PARRISH, et al., In Press) (Figure 6) and dune
sands are very common in the broad equatorial humid zone in the data available for the
Early Jurassic.
CONCLUSIONS
Rocks of the Newark Supergroup were deposited during an interval greater than 35
million years, from the Middle Carnian of
the Late Triassic through the Toarcian of
the Early Jurassic. If the oldest beds datable by vertebrates are included, the range
increases to 45 million years. Within this
interval seven pollen and spore zones can be
recognized and these allow the Newark to be
correlated with the European standard stages
and published radiometric scales.
Correlation by vertebrates is especially
useful within the Newark and within areas of
continental sedimentation where palynomorph
data are lacking. Using all the available data, it appears that a number of sequences
thought to be Late Triassic in age are actually Early Jurassic.
These correlations permit the conclusion
that the transition from Late Triassic to
Early Jurassic was marked by a strong decrease
in floral and faunal provinciality and an increase in indicators of aridity in the equatorial zone.
ACKNOWLEGEMENTS
The principal palynoloqical research for
79
this paper was orginally part of the senior
author's Ph.D. thesis at The Pennsylvania State
University under Dr. ALFRED TRAVERSE and this
work was supported in part by National Science
Foundation grant number GA36870 to Dr. TRAVERSE. The junior author's contribution was produced while a Miller Postdoctoral Fellow at
University of California at Berkeley and support from the Miller Institute for Basic Research is gratefully acknowleqed. We also
thank Dr. KEVIN PADIAN for reading the manuscript and for providing many helpful suggestions which substantially improved it.
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