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20
TITLE
PER EEK ER
nd ee Er

REINER

EN

REN her ee

er natne.

a z

rs Som

ER N Re

et
Stuttgarter Beiträge zur Naturkunde

Herausgegeben vom
Staatlichen Museum für Naturkunde in et

yon
I ven ee E vn
a rg 4,0

Serie B (Geologie und Paläontologie), Nr. 26 LIBRAR en 1977

The ""White’’ (Upper) Jurässie >

in Southern Germany

Dr

By Bernhard Ziegler, Stuttgart

With 11 plates and 42 figures

1. Introduction

The upper part of the Jurassic sequence in southern Germany is named the
“White Jurassic“ due to the light colour of its rocks. It does not correspond exactly
to the Upper Jurassic as defined by the International Colloquium on the Jurassic
System in Luxembourg (1962), because the lower Oxfordian is included in the
“Brown Jurassic“, and because the upper Tithonian is missing.

The White Jurassic covers more than 10 000 square kilometers between the
upper Main river near Staffelstein in northern Bavaria and the Swiss border west of
the lake of Konstanz. It builds up the Swabian and the Franconian Alb. Because
the upper Jurassic consists mainly of light limestones and calcareous marls which
are more resistent to the erosion than the clays and marls of the underlying Brown
(middle) Jurassic it forms a steep escarpment directed to the west and northwest.
To the south the White Jurassic dips below the Tertiary beds of the Molasse trough.

2. Lithostratigraphy
Ye ne Syzerlsireim Aue

The lithostratigraphical sequence of the upper part of the Jurassic in southern
Germany was first studied in detail in the Swabian Alb by F. A. QuenstepT (1843).
He introduced symbols (a to £) for six main lithostratigraphic units which are still
in use.

The so-called White Jurassic « is a rather marly formation. Its lower part is
defined by a series of about ten grey limestone beds (“Grenzbank“ of ©. Fraas

Stuttgarter Beitr. Naturk., Ser. B, Nr. 26 Stuttgart, 30. 6. 1977

2 STUTTGARTER BEITRÄGE ZUR NATURKUNDE Ser. B, Nr. 26

Lichtenfels
Staffelstein

Ze |
S Bamberg = a
.. S =
Würzburg
es)
IE
= Erlangen /@
Hartmannshof !
Nürnberg ® |
zZ
o
z I,
Sn SE
U
Weissenburg | ar Regensburg |
i i BEıc=ı F[Üü GE — i
Heıdenheım am Hahnenkamm = sel ecchtlingen =
ee
Aalen, Lo ofen SE ichs Kelheim |
Stuttgart SS a. Er
= I =8Nattheim> Neuburg an der Donau
en Heiadenheım an der Brenz
ne a Geislingenan.der-Steige
Reutlingen X me

==Blaubeuren =

Balıngen ®

0 20 40 60 80 100 km
| ___ SuM U GMMEE 7AMMME USE 7 men

Fig. 1. .Schematic map of the distribution of the “White“ (upper) Jurassic in southern Germany.

L: northern Franconian Alb, 2: central Franconian Alb,

3: southern Franconian Alb, 4: Ries, 5: eastern Swabian Alb,
6: central Swabian Alb, 7: southwestern Swabian Alb,

8: Randen, 9: Klettgau, 10: Hegau.

1882, p. 124; see also F. A. QuensTeDT 1858, p. 574, G. Wunprt 1883, p. 151, and
A.J. A. Zakrzewskı 1887, p. 95). In the southwesternmost part of the Swabian Alb
(near Blumberg) these beds are replaced by sponge biostromes. Marls and clays "
immediately below the limestones and biostromes contain fossils of the lower
Oxfordian. They are included into the White Jurassic by A. Zeıss (1957, p. 197)
and subsequent authors. Here they are classified as uppermost Brown Jurassic &
according to the original usage.

The basal limestones of the White Jurassic « are followed by grey marls. Except
for the lowermost part they are characterized by weathered ferrugineous (originally

ZIEGLER, THE WHITE JURASSIC IN S GERMANY 3

& >= 5 ß z hal 2;
Sn Zi

IN = 5 ynuupy, I l
INecKan DIE U I DEE SR Heidenheim
= ZT IN hi z IT N
Stuttgart N 2 BEI RR NR
? a? gg = Fi

! m BL
Dr eG a

Rah

a4 I: Im
en BEN
Ssph,/
O

SO /
„EF \Ehingen

Ä & “—
Reutlingen ZS RR insingen”
N re er

1a; a
Q

N Be ringe —
1 RE,
Is W
N Anden
ES

re

Schaffhausen

Fig. 2. The tableland of the Swabian Alb (shaded: “White“ Jurassic) and its erosional slope in
the north and northwest. View from the south. After A. KocH in G. WAGNER (1960).

pyritic) small nodules. The upper part of the White Jurassic « is built up by marls
and limestones which are replaced in the southwestern part of the Swabian Alb by
sponge biostromes and bioherms named the Lochen beds. The total thickness of the
White Jurassic @ varies between 25 m (in the southwest) and 100 m (in the central
and eastern parts of the Swabian Alb).

The White Jurassic ö# was named by F. A. Quenstept the “well bedded lime-
stones“. It is a rather uniform series of limestone beds separated by thin layers of
marl. As it was shown by E. SeısoLp (1950, p. 294) in the upper part of the forma-
tion individual beds can be correlated over large distances. In some places sponge
bioherms are intercalated in this sequence. In the southwestern part of the Swabian
Alb biostromes and bioherms are the predominant representations of this formation.
The thickness of the White Jurassic £ is about 30 m in the central and eastern parts
of the Swabian Alb. It reaches up to 100 m in the southwest.

The White Jurassic y is once more a rather marly formation. Its lithostrati-
graphic subdivision was studied by H. Aıpincer (1945, p. 112, 143) and O. F.

4 STUTTGARTER BEITRÄGE ZUR NATURKUNDE Ser. B, Nr. 26

o Gregoryceras Spp:
o Glochıceras subclausum
® Perısphinctes parandıeri

e Quenstedtoceras lamberti

o®o

Winzingen nu

Burladıngen

a8 w® Lautlingen

20 30 40 50km \

SR |
er |

5» Blumberg

Fig. 3. The sequence at the limit “Brown“/“White“ Jurassic in the central and southwestern parts!
of the Swabian Alb. |

1: Base of the “White“ Jurassic according to F. A. QUENSTEDT, O. FrAAs, G. WUNDT,
and A. J. A. ZAKRZEWSKI.
|

ZIEGLER, THE WHITE JURASSIC IN S GERMANY 5

GEYER (1961a, p. 105). More calcareous beds are intercalated few meters above the
base of the formation, at the base of its upper part, and within the upper part. These
calcareous members can be traced as a whole, but not as individual beds, from the
southwest to the east all over the Swabian Alb. As in the White Jurassic $ in some
localities small sponge bioherms occur within the sequence. Especially the calcareous
horizon at the base of the upper part of the White Jurassic y is often represented by
sponge limestones. The thickness of the White Jurassic y is largest in the central
part of the Swabian Alb (55 to 65 m). Towards the east (Aalen: 35 m) and the
southwest (Tuttlingen: 20 m) the thickness is considerably less.

The White Jurassic ö is represented by bedded limestones. The lithostratigraphi-
cal subdivision was established by H. Aıpinger (1945, p. 112) and refined by
B. ZiesLer (1955, p. 40). As in the White Jurassic £ individual beds can be traced
over large distances (B. ZiEGLER 1958a, p. 266). The lowermost meters of the forma-
tion are rather thin bedded. Then a more marly sequence follows. The middle part
is once more rather thin bedded whilst the upper part of the formation is built up
by thick bedded limestones without layers of marl. A marker bed (Glauconite marker
bed) separates the middle from the upper part of the White Jurassic ö. Approximately
at the same horizon the sponge limestones spread over most parts of the Swabian
Alb. The mean thickness of the White Jurassic ö is in the central part of the Swabian
Alb about 50 meters, in the east and the southwest somewhat less.

The White Jurassic e was originally established by F. A. Quenstept (1843,
p. 447) for unbedded limestones and dolomites of the upper White Jurassic. In
addition he thought silifications to be characteristic of this formation. In the
meantime it became clear that the massive limestones are of rather different ages.
They range from the White Jurassic ö to the White Jurassic £ and originated in the
extensive growth of algal-sponge bioherms. Silification, too, is not of stratigraphic
value. The existence of bedded limestones contemporaneous to the massive lime-
stones was first dicovered by TH. SCHMIERER (1902, p. 542) and studied in detail by
F. BERCKHEMER (1922) and A. Roır (1931). They-are characterized by a light, some-
what brownish colour and are usually thin bedded. Marly layers are missing. A
correlation of individual beds over large distances is not possible. Although the
bulk of the unbedded limestones starts with the upper part of the White Jurassic ö
the White Jurassic & is now restricted to parts of these rocks and to its bedded equi-
valents. The mean thickness of the White Jurassic & in the revised sense is about
20 to 30 meters.

The White Jurassic © comprises the more marly sediments above the pure lime-
stones of the White Jurassic & in the Swabian Alb. Their lithostratigraphic sub-

2: Base of the “White“ Jurassic, according to A. Zeıss, H. HÖLDER, and O. F. GEYER &
M. P. GWINNER.

Section Blumberg after A. Zeıss (1955), G. HAUERSTEIN (1966), and R. GycI (1969).
Section Lautlingen after A. J. A, ZAKRZEWSKI (1887). Section Burladingen after W. HAHN
& U. KoERNER (1971). Section Reutlingen after K. SCHÄDEL in H. HÖLDER (1964). Section
Glems after A. TERZIDIS (1966). Section Bad Boll after H. SöLL (1954). Section Winzingen
after G. STAHLECKER (1934).

6 STUTTGARTER BEITRÄGE ZUR NATURKUNDE Ser. B, Nr. 26

get |
Heidenheim am |
Hahnenkamm |

/

Essıngen

en

Gosheım

[)
ä
Fig. 4. The lithostratigraphy of the uppermost part of the White Jurassic a.

Sections Gosheim, Sauserbrunnen, Pfeffinger Böllat, Ringingen, and Genkingen after U.

KOERNER (1963). Section Neuffen after E. & I. SEIBOLD (1953). Sections Bosler, a |
and Heidenheim am Hahnenkamm after H. SCHMIDT-KALER (1962 b).

EFT EEE

ZIEGLER, THE WHITE JURASSIC IN S GERMANY ; 7

|
|
|

_—

AIEHRTERIH
ÄRREIRETENEN
NEHHHFSHTEIN

HAHN
Hin
in

1

= Lauchheim

\ Unterkochen & Si
g Zee > 5,
.Osterbuch] an

= [ Essingen

ec oe oe

Donau

I

Fig. 5. The lithostratigraphy of the White Jurassic # at the section of Neuffen (after E. & 1. Seı-
BOLD 1953), and the correlation of individual beds in the eastern Swabian Alb (after E.

SEIBOLD 1950).

8 STUTTGARTER BEITRÄGE ZUR NATURKUNDE Ser. B, Nr. 26

N BE 5 SW) 160, 50
N RE s a NE“

\ ae @ IS
ES N „eu
—— Ai l =
-— 730
= sQ, =

6 88km

Fig. 6. The thickness of the White Jurassic # in the Swabian Alb.
Isopachs after E. DIETERICH (1940), modified after R. Gyci (1969) for Klettgau, Randen,
and southwesternmost Swabian Alb, D. ELwERT (1963), H. GEBERT (1964), and G. HAFNER
(1969) for the southwestern part of the Swabian Alb, E. WıRTH (1958; 1960) for the bore-
holes Buttenhausen, Upflamör, and Ehingen, and E. SEIBOLD (1950), M. BEURER (1963),
and W. SCHALL (1964) for the eastern part of the Swabian Alb.

division was established by A. Roır (1931). In the bedded facies it starts with
irregularly bedded limestones alternating with marly layers. This member is named
the “Liegende Bankkalke“ and reaches a thickness of about 30 to 50 meters (in the
eastern part of the Swabian Alb up to 100 m). At some localities in the central and |
southwestern Swabian Alb the limestones pass laterally into calcareous shales (e. g.
Nusplingen). The “Liegende Bankkalke“ are followed in some restricted areas by
the Cement marls which attain a thickness up to 120 meters. The uppermost unit in |
the Swabian Alb is named the “Hangende Bankkalke“. They are represented by an
alternation of irregularly bedded limestones and marly layers. Because they are

ZIEGLER, THE WHITE JURASSIC IN S GERMANY

ALDINGER | GEYER
1945 1961
% d
—-

Yamk
1
E3m
I
Der

In

Erkenbrechtsweiler

=

Drackenstein

Y2
Z—
es Zn
I a
(else I
„ x
Fe [= SE = ya
Br Y’mo A — Een —
— A an Br — N on
Rt Me
jem—nun Y! Y mu E ale ei zen
vövF ® =— al 2 A Br — —— — a
nn) == (nam me Sn
en: 2 z Neuffen Erkenbrechts-- Hochwang Geislingen
weıler
Geislingen

@

en

aß
Erkenbrechtsweiler, N
Neuffe “ Boch
©

Drackenstein

Neckar
Fig. 7. The lithostratigraphy of the White Jurassic / in the central part of the Swabian Alb. After

H. ALDINGER (1945) and O. F. GEYER (1961 a).

Donau

10 STUTTGARTER BEITRÄGE ZUR NATURKUNDE Ser. B, Nr. 26

m
9
8
7
6 T Wweißenstein
5 <
4 “T) eislingen
3
2

Neckar

murs

Em: —= normal facıes dominating

wo sponge facıes dominating
o 30 40 50km in White Jurassic &>
IT
Fig. 8. The lihostratigraphy of the lower part of the White Jurassic ö in the Swabian Alb. Note

the more marly sequence of the White Jurassic ö2 in the Urach region (sections Unter-
hausen, Sirchingen, Neuffen, and Schlattstall). After B. ZIEGLER (1955; 1959).

ZIEGLER, THE WHITE JURASSIC IN S GERMANY

| 5
ee — — zn =

\

3

2

+

RL

\E
ax gun &
) Röttingen
FAR) nr
oo 7
Ih Weissenstein
FE
Y Schlattstall
0% I Hülben
Sirchingen
Unterhausen
\ Genkıngen
2 Ü ®@ Stetten unter Holstein
Da
mr

[INS BL CO BEE ge 1 BL cn N Ei Co Co)

—

Neckar

Tuttlingen

11

Fig. 9. The lithostratigraphy of the middle part of the White Jurassic 6 in the Swabian Alb. After

B. ZIEGLER (1955; 1958 a; 1959).

12 STUTTGARTER BEITRÄGE ZUR NATURKUNDE Ser. B, Nr. 26

0

Sections near Grabenstetten
(Central Swabıan Alb):

Fig. 10. The different interpretations of the White Jurassic e. Stippled: The White Jurassic & accor-
ding to F. A. QuEnsteprt. Shaded: The White Jurassic & as the term is used today. After
©. F. GEYER & M. P. GwinnERr (1961). Section Grabenstetten after F. BERCKHEMER & H.
HÖLDER (1959).

eroded more or less their original thickness is not known but must have exceeded
100 meters. All these beds are locally replaced by biostromes and bioherms, mostly
built up by sponges, sometimes — in the “Liegende Bankkalke“ and the Cement
marls — by corals. The lithostratigraphic relationships of the White Jurassic { are
best summarized by M. P. Gwinner (1976, p. 17).

2.2. The Eranconian Alb

The upper Jurassic sequence in the Franconian Alb resembles that of the Swa-
bian Alb. In the lower and middle part of the upper Jurassic — corresponding to the
Swabian White Jurassic « to ö — three basins with minor differences in sedimen-
tation are recognized (A. Zeıss 1968a). The basins are separated by algal-sponge
bioherms. In the northernmost basin the greatest affınities to the sedimentation of
the Swabian Alb are present. In the other basins the sediments are more calcareous,

Fig. 11. The lithostratigraphy of the White Jurassic £.
Section Engen after A. SCHREINER (1961). Section Sigmaringen (combined section) after
A. Rott (1931) and J. SCHNEIDER (1957). Section Zwiefalten after H. W. HAAG (1960)
and J. SCHNEIDER (1957). Sections Grabenstetten and Münsingen after J. SCHNEIDER
(1957). Sections Schelklingen and Blaubeuren after W. LirzIcH (1962) and J. SCHNEIDER
(1957). Sections Mergelstetten and Neresheim after M. BEURER (1963), K. KNoBLICH
(1963), W. REıFF (1958), and J. SCHNEIDER (1957).

ZIEGLER, THE WHITE JURASSIC IN S GERMANY 13

Neresheım

: =
Mergelstetten

GE Maın outcrops of the White Jurassıc %

Sıgmarıngen 03 - „Hangende Bankkalke”
62 = Cement Marls
ZK = „Zwischenkalke"

2 = „Liegende Bankkalke”
0 10 20 30 40 50 60km
Ts Bi EEE

14 STUTTGARTER BEITRÄGE ZUR NATURKUNDE Ser. B, Nr. 26

especially in the more marly formations. Correlation of individual beds is possible
within each basin (B. v. FREYBERG 1966) but difficult between different basins.

Pecularities in the Franconian Alb are the Treuchtlingen “marble“, a thick
bedded calcareous formation restricted to the Southern Franconian Alb and equi-
valent approximately to the Swabian White Jurassic ö, and the “Franken-Dolomit“.
This latter formation is built up by sometimes massive, sometimes stratifiied dolo-
mites which correspond to the massive limestones of the Swabian White Jurassic :
and uppermost ö but sometimes apparently include even lower strata. Thus the
“Franken-Dolomit“ especially in the southern Franconian Alb partly overlies and
partly is equivalent to the Treuchtlingen “marble“ (U. Bantz 1970; R. MEyErR |
1972ER 974: om):

It is the upper part of the upper Jurassic for which especially the southern Fran-
conian Alb is famous. A summary was given by B. v. FREyYBERG (1968) and A. Zeıss
(1968a, p. 103; 1968b, p. 17). The sequence above the Treuchtlingen “marble“ and
the “Franken-Dolomit“, respectively, starts with pure, bedded limestones. Locally
silifications are frequent. These series, which are named the Torleite beds and the
Geisental beds, are followed by the well known Solnhofen calcareous shales and
by the Mörnsheim beds which resemble the Solnhofen shales but contain much
more silica. The sequence continues with the Usseltal formation (bedded limestones
and calcareous shales) and the Rennertshofen formation. All these strata together
attain a maximum thickness of about 400 meters, that is more than twice the
thickness of all the formations corresponding to the Swabian White Jurassic «a to d.

In a very restricted area near Neuburg an der Donau the youngest sediments of
the Franconian Jurassic are exposed. This Neuburg formation contains white, so-
mewhat marly limestones and is about 45 meters thick (K. W. BARTHEL 1962; 1969).

Between Regensburg and Passau small outcrops of upper Jurassic sediments are
known (L. v. Ammon 1875). However, they will not be mentioned further. For
references on the upper Jurassic in Franconia see B. v. FREYBERG (1974), E. FrüceL
(edit., 1975, p. 154, 212), and A. Zeıss (1977).

23 Ihres Up; press RahtiomresaVzayllresy,

In the Upper Rhine Valley between Basel and Freiburg some outcrops of tecto-
nically isolated upper Jurassic rocks are known. Because they belong to the so-called |
rauracic facies belt they will not be treated in this context.

3. Biostratigraphy

The biostratigraphy of the White Jurassic sequence in southern Germany is
based mainly on ammonites. Other macrofossils and foraminifera are of less value.
Ostracods are not yet studied. Ammonites are rather frequent and a great variety
of genera and species is present. It has been found that perisphinctids and aspido-
ceratids are the best index fossils, the range of haploceratids in most cases being
much larger.

Weissenburg

| S. platynota

\ S.galar

I,planula

E.bimammatum

ZIEGLER, THE WHITE JURASSIC IN S GERMANY 15
Ebermannstadt Hartmannshof
|
S.platynota S.platynota
= RR == a
m S 7

= m Sgalar = Se
=

je}

E

=

se

SZ I,planula
= =

=

—_
me j Iplanula
— ==

==

>

I

Fe]

== | E.bımammatum

E.berrense

0) 20 40 60 80 00 km
EEE EEE ug er En

Pmmaı

l E.berrense

| E.berrense

D. bifurcatus

Fig. 12. The three sedimentary basins in the lower Malm of the Franconian Alb and sections charac-

teristic for them.

Ebermannstadt: northern Franconian Alb; Hartmannshof: central Franconian Alb; Weissen-
burg: southern Franconian Alb. Cross-hached: eastern Swabian Alb. After B. v. FREYBERG
(1966) and A. Zeiss (1968 a).

16 STUTTGARTER BEITRÄGE ZUR NATURKUNDE Ser. B, Nr. 26

Solnhofen

Wettelsheım Om

—I

Treuchtlingen
|

Dietfurt

Wettel en
Treuchtlingen

Wemdıing

Fig. 13. The correlation of individual beds in the Treuchtlingen “marble“, according to H. SCHMIDT-
KALER (1962 b, and personal communication).

17

supposed equiva-
lents ın the

Swabıan Alb:

fresh water
indications:
extension of
reef sedıments:

I—

Marls

E

emen

dno.b JelIynW)Y

Usseltal formatıon

ZIEGLER, THE WHITE JURASSIC IN S GERMANY
Neuburg formation
Rennertshofen formatıon
Mörnsheım formatıon

Oberhausen member
Unterhausen member
Fınkensteın member
Ammerfeld member
Bertholdsheım member
Storzelmühle member
Gansheım member
Spindeltal member
Tagmersheiım member

Solnhofen formatıon

al U
m N
Seo
eo 0 |o
@

a S |e
g|S 8

&
SS ld
e| on |S
5 |e
<Sı © |
lei
DI |

Geisental (Röglıng)) formatıon
Torleite formatıon

Lower Solnhofen beds

conian Alb. After A. Zeiss (1968 a; 1968 b; 1977).

Fig. 14. The lithostratigraphic sequence in the upper Malm of the southwestern part of the Fran-

Ser. B, Nr. 26

STUTTGARTER BEITRÄGE ZUR NATURKUNDE

18

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Fig. 15. Main index fossils of the White Jurassic of the Swabian Alb. After I.G. Sarunov & B.
ZIEGLER (1976).

ZIEGLER, THE WHITE JURASSIC IN S GERMANY 19

Be
Rıngsteadıa

Sutneria platynota

- u
en |
zo
Bee .Q |!
2 Ku
| S ||
Zum 3 n 25
— 5
== 418 s:
An ze < il)
< ©
2 11 ‚So
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S 1 &
S S ö
2 | KU
S
| £ |
<
| Z | |
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&
S
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fi

Amoeboceras alternans and ovale

BEE Discosphinctes streichenensis

Taramelliceras pichleri and lochense

Glochiıceras mıcrodomum
Taramellıceras tenuınodosum
Taramelliceras wenzeli

Glochiceras canale

|
Ohosphinctes colubrinus, polygyratus and tızıanı

Amoeboceras bauhinı

>
u
I
Q
&
x
u
U
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u)
U
ID
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U
Sy
Q
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&
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Glochiceras lingulatum
Taramellıceras hauffıanum
Taramellıceras lıtocerum

N

Fig. 16. Ranges of some ammonites in the uppermost White Jurassic «a and in the White Jurassic £
in the Swabian Alb. Mainly after E. DIETERICH (1940) and U. KOERNER (1963).

Physodoceras altenense and circumspınosum

3.1. The Swabian Alb

In the Swabian Alb the base of the White Jurassic @ is characterized by Grego-
tyceras transversarium and G. toucasianum. Unfortunately both species are very
rare. However, Glochiceras subclausum, Ochetoceras canaliculatum, and O. hispidum
are valuable substitutes. Somewhat above follows a horizon with Dichotomoceras
bifurcatus. This zone is proven only at very few localities, owing to difficulties in

20 STUTTGARTER BEITRÄGE ZUR NATURKUNDE Ser. B, Nr. 26

preservation. In the marls of the middle White Jurassic « no ammonite species
restricted to these beds is known, but the brachiopod species Aulacothyris impressa
is a useful marker. Amoeboceras alternans is used as index fossil. It occurs, how-
ever, in the upper part of the White Jurassic « and in the Lochen beds, too. In the
upper part of the White Jurassic a Epipeltoceras bimammatum occurs, but is very
rare. More frequent species characteristic for these beds are Glochiceras canale,
G. microdomum, and Taramelliceras pichleri. Ringsteadia is proven but is not very
frequent.

The White Jurassic £ is characterized by Idoceras planula and its relatives.
Idoceras is known to start with the lowermost layers of the formation and Epipel-
toceras bimammatum is said to occur still in the same beds. Thus, their ranges seem
to overlap for a short interval. Within the White Jurassic ß# E. DieTEricH (1940,
p. 8) established a refined biostratigraphy using small species of Taramelliceras. In
practice, however, there are great difficulties in the application of these species. In
the uppermost few meters of the White Jurassic £ I. planula is said still to occur.
More important as an index fossil for these beds is Sutneria galar. It is accompanied
by species of Physodoceras (P. altenense and P. circumspinosum) which, however,
are found in the overlying strata, too. Ringsteadia is proven throughout the White
Jurassic ß, but is rare.

Immediately above the boundary between the White Jurassic ßf and y Sutneria
platynota sets in. In this zone Ataxioceras makes its appearance. Somewhat above
the limestones of the lower White Jurassic y S. platynota is replaced by S. cyclodor-
sata. Only few meters higher Streblites tenuilobatus and Creniceras dentatum occur
for the first time, and Ataxioceras (subgenus Parataxioceras) reaches its climax.
Ataxioceras (subgenus Ataxioceras) has its greatest development in the upper region
of the middle part of the White Jurassic y. Other species characteristic for the middle

part of the White Jurassic y are Taramelliceras (Metahaploceras) strombecki and

Aspidoceras binodum. Rasenia is not rare. The upper White Jurassic y is characte-
rized by “Katroliceras“ divisum and related species and by Aspidoceras uhlandi.

Streblites tenuilobatus, Creniceras dentatum, and Rasenia still are present. Another

characteristic species in these beds is Taramelliceras trachinotum. Nebrodites, al-
though present much earlier, becomes rather frequent. Idoceras balderum is an ex-
cellent marker for a group of limestone beds within the upper part of the White
Jurassic y. For full details on the zonation of the formation see ©. F. GEYER 1961 a,
p. 107).

The uppermost beds of the White Jurassic y and the lowest part of the White
Jurassic ö contain Lithacoceras ribeiroi. Aulacostephanus eulepidus is characteristic
of the lower limestones and calcareous marls of the White Jurassic 6. The species
is missing in the lowermost beds of the formation, but is still present in the lowest
parts of the thin bedded limestones of the middle White Jurassic ö. A. mutabilis is
known from the same beds as A. eulepidus but is very rare. Aspidoceras acanthicum
which is found already in the uppermost beds of the White Jurassic y is another
index fossil for the lower part of the White Jurassic ö. Streblites tennilobatus is
replaced by S. levipictus. Creniceras dentatum and Sutneria cyclodorsata are still
present. Nebrodites is rather frequent, too. In the middle and upper part of the White
Jurassic ö Aulacostephanus eudoxus and A. pseudomutabilis are characteristic. In

21

ZIEGLER, THE WHITE JURASSIC IN S GERMANY

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GEYER (1961 a; 1961 b).

the lower part of their ranges Streblites levipictus, Creniceras dentatum, and Sutneria
cyclodorsata still occur. The same beds are characterized by Orthaspidoceras (O.

liparum and O. schilleri). All these species suddenly disappear few meters below the

22 STUTTGARTER BEITRÄGE ZUR NATURKUNDE Ser. B, Nr. 26

le 2 RA
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S| man eumela

Fig. 18. Ranges of some ammenites in the White Jurassic ö in the Swabian Alb. Mainly after B.
ZIEGLER (1958 b; 1962).

glauconite marker bed. Sutneria cyclodorsata is replaced by S. eumela which is
restricted to the upper part of the range of Aulacostephanus eudoxus. |

At the limit between the White Jurassic ö and e A. eudoxus and A. psenudo-
mutabilis disappear. New species are Sutneria pedinopleura and Hybonoticeras pres-
sulum. Both are recorded only from very few localities (see D. SEEGER 1961, p. 57),
and are followed only few meters higher by S. subeumela and H. beckeri. Aspido-
ceras hermanni is characteristic of the range of Sutneria subeumela. The index fossil

ZIEGLER, THE WHITE JURASSIC IN S GERMANY 23

„Hangende
Bankkalke”

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Hmundulum

Fig. 19. Ranges of some ammonites in the White Jurassic & and Z in the Swabian Alb. Mainly after
F. BERCKHEMER & H. HÖLDER (1959) and D. SEEGER (1961), slightly modified.

for the upper part of the White Jurassic e is Virgataxioceras setatum. This species is
accompanied by Taramelliceras wepferi and Hybonoticeras beckeri. However, both
species still occur in the lower part of the White Jurassic £.

The biostratigraphy of the White Jurassic £, summarized by F. BERCKHEMER &
H. HöLper (1959, p. 114), is very uncertain, owing to the scarcity of ammonites
except uncharacteristic species of Glochiceras and Taramelliceras. For the “Liegende
Bankkalke“ Lithacoceras ulmense and Subplanitoides siliceus are used as index
fossils. Their ranges are, however, not well defined. Hybonoticeras beckeri is said to
be found in rather young beds of the “Liegende Bankkalke“. From the upper part
of this member and from the “Hangende Bankkalke“ H. hybonotum and Gravesia
are recorded.

3.2. The Franconian Alb

In the lower and middle part of the upper Jurassic sequence the differences in
biostratigraphy between Swabia and Franconia are unimportant. Between Gregory-
ceras transversarinm and Epipeltoceras bimammatum in Franconia beds with Euaspi-
doceras hypselum and a zone with Epipeltoceras berrense can be distinguished.
Contrary to the relationships in Swabia in Franconia Orthaspidoceras liparum is
already known from the strata with Aulacostephanus eulepidus. A. mutabilis is not
known from Franconia (H. SchmiDT-KALER 1962 a; 1962 b).

The biostratigraphy of the uppermost Jurassic in Franconia is known very well
and shows much more details than in Swabia. It has been summarized by A. Zeıss

24 STUTTGARTER BEITRÄGE ZUR NATURKUNDE Ser. B, Nr. 26

Oberhausen S
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Fig. 20. Ranges of some ammonites in the upper Malm of the southern Franconian Alb. Mainly
after K. W. BARTHEL (1962; 1969) and A. Zeıss (1968 b).

(1968b, p. 133). According to this author Hybonoticeras beckeri is restricted to the
Torleite beds. The subdivision of this formation (Sutneria pedinopleura — 5. subeu-
mela — Virgataxioceras setatum) is identical with the relationships in the Swabian
Alb.

From the Geisental beds to the Mörnsheim beds Hybonoticeras hybonotum and
Gravesia are recorded. The index species of the Geisental beds is Lithacoceras rie-
dense. In the Solnhofen shales Subplanites rueppellianus is characteristic. In the
Mörnsheim beds S. moernsheimensis occurs. Neochetoceras steraspis and Glochiceras
lithographicum are known from the Solnhofen shales but are much more frequent in
the Mörnsheim beds.

The zonal sequence in the Usseltal and Rennertshofen formations is based on
relatively few specimens and depends largely on apparently endemic species of the
Perisphinctidae. Only Franconites vimineus is known in somewhat greater number.
It occurs in the middle (and more rarely in the upper) part of the Rennertshofen
formation. Neochetoceras mucronatum is characteristic of the uppermost Mörns-
heim beds, the Usseltal formation, and the lower Rennertshofen formation.

In the Neuburg formation the exact distribution of the Perisphinctidae is not yet
published. Lemencia ciliata and “Isterites“ palmatus are characteristic of the for-
mation as a whole except of the uppermost part. Additional ammonites are Pseudo-
lissoceras bavaricum, Protancyloceras, Simoceras, and Virgatosimoceras. The top-
most beds of the Neuburg formation contain the calpionellid Crassicollaria.

ZIEGLER, THE WHITE JURASSIC IN S GERMANY 25
4. Chronology

Owing to the great number of ammonite species the correlation of the local
range zones with the international standard scheme is well established.

The base of the White Jurassic, that is the zone of Gregoryceras transversarium,
is interpreted by J. H. Carzomon (1964, p. 289) to be contemporaneous with the
base of the upper Oxfordian (cautisnigrae zone). However, R. Gysı (1966, p. 941)
showed that the transversarium beds represent the uppermost part of the plicatilis
zone (parandieri subzone) and sometimes even include the antecedens subzone.
A. Zeıss (1966, p. 110), too, puts the fransversarium zone into the middle Oxfordian.
As is indicated by the occurrence of Ringsteadia in the ranges of Epipeltoceras
bimammatum and Idoceras planula these zones seem to be contemporaneous with
the psendocordata zone. Thus the marls with Aulacothyris impressa may be an
equivalent of the decipiens zone, their lowermost parts perhaps even of the
cautisnigrae zone.

The limit between the White Jurassic # and y seems to be the limit between the
Oxfordian and the Kimmeridgian, as is shown by the distribution of Ringsteadia.
Unfortunately no true Pictonia and no Pachypictonia identical with those of north-
western Europe are known in southwestern Germany. Moreover, Rasenia is found
in the Swabian Alb already in the White Jurassic f, that means in true equivalents
of the pseudocordata zone. Because Rasenia reaches its climax in southern Germany
in the tenuilobatus zone (middle and upper part of the White Jurassic y) there are
good reasons to interpret this period to be an equivalent of the cymodoce zone.
If so the zone of Sutneria platynota is contemporaneous with the baylei zone. This
is confirmed by few findings of Pictonia in the northern Franconian Alb.

Common index fossils in the White Jurassic ö prove that this formation belongs
to the mutabilis and eudoxus zones. The zones of Sutneria subeumela and Virgata-
xioceras setatum were named by E. Hennig (1943, p. 84) the new stage „Suebium“
owing to their very peculiar and endemic faunas. It can be shown, however, that the
White Jurassic & and large parts of the “Liegende Bankkalke“ (that means the range
of Hybonoticeras beckeri) are the local equivalents of the autissiodorensis zone
and therefore the youngest Kimmeridgian s. str. (B. ZIEGLER 1962, p. 26; 1964,
p. 351).

The limit between the Kimmeridgian s. str. and the lower Tithonian falls bet-
ween the ranges of Hybonoticeras beckeri and H. hybonotum, that means it falls
into the upper part of the “Liegende Bankkalke“ in Swabia and into the Geisental
beds in Franconia, respectively. In the Swabian Alb only the uppermost “Liegende
Bankkalke“, the Cement marls, and the “Hangende Bankkalke“ are of Tithonian
age. All these strata belong to the Gravesia zone.

In southern Franconia the lower Tithonian is much more complete. It contains
a considerable number of zones. Therefore, the name “Danubian“ for this substage
may be used. All strata younger than the Mörnsheim beds have no equivalents
in the Swabian Alb.

The Neuburg formation represents the middle Tithonian as it was shown by K.
W. Barrher (1962, p. 23) and K. W. BarTHEL & J. R. GeyssanTt (1973, p. 33) when

26 STUTTGARTER BEITRÄGE ZUR NATURKUNDE Ser. B, Nr. 26

studying the occurrence of Pseudolissoceras, Virgatosimoceras, and other ammonite
genera. Ihe uppermost part of the Neuburg formation is already upper Tithonian in
age as is indicated by the occurrence of the calpionellid Crassicollaria (K. W. Bar-
THEL 1969, p. 150). In the Franconian Alb no marine transition from the Jurassic
into the Cretaceous is known.

5. The normal facies

Fol, unenolog’y

The sediments of the White Jurassic in southern Germany consist of two rather
different units: The so-called normal facies and the sediments of recifal or organic
origin. The sedimentological features of both have been described in detail by M.
P. Gwinner (1976). He, too, refers to the modern literature.

For the normal facies bedded limestones and calcareous marls are characteristic.
The carbonates are lutites. Among the clayey components kaolinite and illite predo-
minate (W. BauscH 1971, p. 333). The sequence is built up by limestone beds of
different thicknesses alternating with more marly layers. As it was shown by E. Seı-
BOLD (1952) and H. Weızer (1957) in the more calcareous formations the amount
of carbonate exceeds 90°/o in the limestone beds and varies between 70°/o and 90°/o
in the marly layers. In the marly formations the limestone beds sometimes contain
only 70-75 ®/o carbonate, the marly horizons being still less calcareous. That means
that the appearance of an individual bed as a limestone or as a marl does not depend
on the absolute but on the relative content of carbonate and that it is the result of
weathering.

In the calcareous formations of the White Jurassic ß (planula zone) and Ö
(acanthicun and lower eudoxus zones) individual beds can be traced over large
distances. This is possible because the carbonate content is constant over large areas,
and each change of sedimentation to more or less carbonate took place simul-
taneously. Moreover, the quantity of precipitated lime and clay is approximately the
same at very different localities. Apparently the oceanographic conditions were very
uniform during these times. The ocean floor was deep enough so that it was not‘
disturbed by currents, waves or storms.

In the upper part of the White Jurassic ö (upper eudoxus zone) and in the White‘
Jurassic & (lower and middle beckeri zone) the limestones are very rich in carbonate
(partly more than 99 %/o). Marly layers are missing. Apparently the influx of clay
minerals that continued during the upper Oxfordian and most parts of the Kimme-
ridgian was interrupted. Many limestone beds contain stylolites, often the surface of
beds is covered with stylolites. Therefore it seems that solution has diminished the
original thickness of the sediments to some degree. Owing to the absence of marly
layers and to the stylolitic structure a correlation of individual beds is impossible.

The limestones of the upper White Jurassic in the Swabian Alb (upper beckeri
zone and Gravesia zone) are bedded rather irregularly. A correlation of individual
beds over considerable distances is impossible. Sometimes the sedimentation is
disturbed by slumping or other unconformities. It seems that the sedimentation took

ZIEGLER, THE WHITE JURASSIC IN S GERMANY 27,

x

TÄHHIA

Inn

70 80 90 100% CaCO, \ 70 60 °0 100% GaC0z
m
o Essingen
oo

Neckar ER
IN Donau
BR 06 a
a OR DE ER eH)em

Fig. 21. Correlation of individual limestone beds over a distance of about 25 km in connection with
the content of calcium carbonate. Upper part of the White Jurassic # of the eastern Swa-

bian Alb. After H. WEILER (1957).

place under a regime of higher energy compared with older beds. Apparently the sea
was shallower.

28 STUTTGARTER BEITRÄGE ZUR NATURKUNDE Ser. B, Nr. 26

m 0 50 100% j >20
FE een L N L f N er, 1 N |

|
Fig. 22. The unsoluble residues in some samples of the Swabian White Jurassic and the sizes of the
grains. After G. KNOBLAUCH (1963). |

——— 0 50 100% 0 500

a (BEBEBEEN ı ı ı l 1 re] ee ne En. _

ZIEGLER, THE WHITE JURASSIC IN S GERMANY 29

The so-called “Treuchtlingen marble“ which is characteristic in the acanthicum
and endoxus zones of southern Franconia shows a special type of sedimentation.
The beds are rather thick and contain a considerable amount of calcified siliceous
sponges. The sponges are covered by calcareous crusts (see page 33) apparently of
algal origin and by sessile miliolid foraminifera. Algal crusts and miliolid foramini-
fera point to sedimentation of the “Treuchtlingen marble“ in rather shallow waters.
On the other hand B. v. FreyBErGg (1966), H. ScHhmipDT-KALer (1962 b), and W.
STREIM 1960; 1961) have shown that the correlation of individual beds is possible
over large distances, so that the sea floor must have been situated below the in-
fluence of currents, storms and waves.

In addition to the carbonates and the clayey components a certain amount
(0,2—2 °/o) of heavy minerals is present within the rocks (G. KnosLAucH 1963). In
most cases the heavy minerals are authigenous, for instance pyrite, haematite,
limonite, apatite, baryte, phosphorite, and others. Other heavy minerals, especially
zirkone, turmaline, and others seem to be terrigenous. Magnetite, pyroxene, and
amphibole are interpreted as to be of volcanic origin. These volcanic minerals
— although present only in very small quantities — are much more frequent and of
larger size in the Oxfordian and the upper parts of the Kimmeridgian (s. str.) than
in the lower Kimmeridgian. Apparently they are wind-blown tuffs.

3.2, Ehe vosetlls

Macrofossils are abundant throughout most parts of the White Jurassic in
southern Germany. The most frequent group are the ammonites. In the Swabian Alb
the Perisphinctaceae are represented by a large number of genera (however, the
distinction between genera, subgenera, and synonyma being highly subjective). The
Haplocerataceae are present with only about one third of the taxonomic units shown
by the Perisphinctaceae. The number of individuals, however, is much larger in the
Haplocerataceae than in the Perisphinctaceae. Only in parts of the Kimmeridgian
(hypselocyclum and divisum zones) in some localities of the normal facies Peri-
sphinctaceae predominate over the Haplocerataceae. Phylloceratids and Iytoceratids
are known only with very few specimens. The Stephanocerataceae are represented by
the amoeboceratids which are rare, however, in the normal facies. No amoeboceratid
is known in southern Germany in strata younger than the upper eudoxus zone.

The most frequent ammonite genera and genus groups in the upper Oxfordian
of the Swabian Alb are the following: Perisphinctids of various generic (or sub-
generic) affinities, mostly microconchs, Taramelliceras, and Glochiceras. Frequent
but restricted to parts of the upper Oxfordian are Idoceras and Trimarginites. Less
frequent are Amoeboceras, Ochetoceras, Epipeltoceras, euaspidoceratids, Physodo-
ceras, Sutneria, Rasenia, and Ringsteadia. Some other genera are known but are
extremely rare.

In the Kimmeridgian of the Swabian Alb the most frequent ammonites belong
to the following genera which, however, in several cases are restricted to parts of

Fig. 23. Heavy minerals in the White Jurassic of the Swabian Alb.
A: Percentage of grains of volcanic material > ec u (black). Authigenous minerals and
magnetite omitted.
B: Maximal diameter of grains. Volcanic material in black.
After G. KNOBLAUCH (1963).

30 STUTTGARTER BEITRÄGE ZUR NATURKUNDE Ser. B, Nr. 26

the stage: Progeronia, Orthosphinctes, Ataxioceras, Aspidoceras, Taramelliceras,
Glochiceras, Creniceras, and Streblites. Less frequent are Amoeboceras, Lithacoceras,
Katroliceras, Rasenia, Aulacostephanus, Sutneria, Nebrodites, Idoceras, Virgataxio- |
ceras, Subplanitoides, Physodoceras, Orthaspidoceras, Ochetoceras, Haploceras, and
Oxyoppelia. All other genera are extremely rare.

The lower Tithonian of the Swabian Alb is very poor in ammonites.

Other macrofossils than ammonites are present with different groups in the
normal facies of the Swabian White Jurassic. They are, however, much less frequent
than the ammonites. The brachiopods are playing a major role. They are represented
by Terebratulida and Rhynchonellida of different generic affinities. The most fre- |
quent genera are Aulacothyris (in the upper Oxfordian), Loboidothyris, and Lacu-
nosella. Terebratulina and other genera of the Terebratulida are well represented,
too. Because brachiopods are a consistent element in the recifal facies and because
they may be allochthonous in some cases it is often difficult to attribute them to the '
normal facies with certainty.

Belemnites range throughout the White Jurassic, being not frequent, however.
In the lower Tithonian they become still more scarce. Nautiloids are always rare,
too. The pelecypods are still scarcer than brachiopods or belemnites, except for some
strata in the lower Tithonian where astartids are rather abundant and for a few
horizons in the divisum zone (Kimmeridgian) which are built up locally nearly |
completely by the shells of Meleagrinella. In the pelecypod epifaunas single valves
of Liostrea roemeri and Velata velata are known from many localities pointing to
formerly attached animals. Limids are present, too. Other epifaunal pelecypods are
scarce. In the infaunal groups Pholadomya acuminata is a characteristic species.
Other species are very scarce.

The gastropods are represented especially by rare specimens of Bathrotomaria.
Crustaceans are scarce except for some parts of the lower Tithonian which are known |
as “Krebsscheren-Kalke“ (that means limestones with crustacean chelipeds). Proso-
pon is an often cited genus in these beds. Crinoids are recorded in the normal facies
from different horizons and localities, their skeletons, however, are mostly totally
disintegrated. The most frequent genus seems to be Balanocrinus. Echinids are
scarce in the normal facies except for a few localities where Collyrites, Holectypus,
and some other genera are present.

Even vertebrates are known, but they are very rare. Mostly only single bones or
teeth of fishes and ichthyosaurians occur. The most important discovery is a skeleton
of Machimosaurus in the hypselocyclum zone (Kimmeridgian).

Trace fossils are present in the normal facies of the Swabian White Jurassic but
are predominantly restricted to few horizons and otherwise rare. The most important !
beds with trace fossils (especially Chondrites) occur in the uppermost part of the |
bimammatum zone and in some parts of the lower Tithonian.

In Franconia the macrofossils of the normal facies of the upper Oxfordian and !
the Kimmeridgian belong to the same groups and genera as in Swabia. In the |
ammonites, however, the Perisphinctaceae seem to predominate the Haplocerataceae |
not only in the number of taxa but also in the number of specimens. In the lower !
Tithonian the differences between Franconia and Swabia became much more obvious
being related, however, to the development of the recifal facies. Therefore the macro- |
fossils of the Franconian lower Tithonian will be treated in the chapter on the
recifal facies.

ZIEGLER, THE WHITE JURASSIC IN S GERMANY 31

Among the microfossils of the upper Jurassic in southern Germany several
groups are rather well studied, the knowledge about other taxa being still incom-
plete. Coccolithophorida are proven (E. Frücer & H.E. Franz 1967, H. Krupp 1976),
but detailed investigations for most parts of the upper Jurassic are still missing.
The dinoflagellates are published by K. W. Krement (1960). Radiolarians are
extremely rare.

Foraminifera are frequent but difficult to extract from the limestones and there-
fore better known in the marly formations. E. & I. SeıwoLp (1960), J. Tu. Groıss
(1966a, 1966b, 1967, 1970) and B. WINTER (1970) record a majority of Nodosaria-
cea (especially of the genus Lenticulina), followed by Lituolacea. Furthermore, repre-
sentatives of the Ammodiscacea, Miliolacea, Involutinidae, and Epistominidae are
present. Some of the species are restricted to a certain amount of carbonate (E. &
I. SEIBOLD 1960, p. 408), others show some variation in their morphology during
their ranges (J. Tu. Groiss 1966 b, 1970).

Sponges are characteristic of the recifal facies. In some localities, however,
isolated spicules occur pointing to the existence of siliceous sponges of choristid
type in the normal facies, too.

The ostracod fauna of the upper Jurassic in southern Germany is much less
known than the foraminifers. Especially in the limestones the fossils are difficult to
extract and often badly preserved. In the Oxfordian (H. GLAsHorF 1964, p. 55) and
in the middle Tithonian (H. OertLı 1965, p. 127) rather poor ostracod faunas are
described. The ostracods of the Kimmeridgian still are not investigated in detail.

6. The recifal and related facies
Gelee uhren sipiommtezer aulleza ln brikorhresumes
In the White Jurassic of southern Germany large areas are covered by the
famous sponge-algal bioherms (“Schwamm-Stotzen“). Their sedimentology was

described in much detail by M. P. Gwinner (1976). Therefore here only the general
relationships will be treated.

Calcareous crusts Foramınıfers

_.

ÄAREE

De x c
Sılıceous sponge I ernten organısms Channel system

0 / 2 IcM

Fig. 24. Cross section through a siliceous sponge (dotted) covered by calcareous crusts and settled
on its lower surface by sessile organisms. After G. K. FRITZ (1958).

32 STUTTGARTER BEITRÄGE ZUR NATURKUNDE Ser. B, Nr. 26

1lle2

Fig. 25. A small sponge-algal bioherm (shaded) evolving during the deposition of a calcareous marl.
White Jurassic ö1 Ile1, Sirchingen near Urach (central Swabian Alb). Note the enlarged
thickness of the bioherm and its being sunken into the underlying bed. After B. ZIEGLER
(1955).

area of normal facıes

sponge-algal bioherm
slope of the bioherm

culminatıon of the bioherm

basıns wıth unsettled sea floor
developing ın elevated

levels of the bioherm er N _
(‚Sekundar-Schüsseln‘) DENE
spreadıng bıoherms

(„Restlücke*)

Fig. 26. The architecture of sponge-algal reefs. After K. SCHÄDEL (1962).

ZIEGLER, THE WHITE JURASSIC IN S GERMANY 33

The framework of the sponge-algal bioherms is formed by siliceous sponges. In
the Oxfordian and Kimmeridgian Hexactinellida are dominating; in the lower
Tithonian the Demospongea became more frequent. The spicular skeletons of these
sponges are covered on their upper surfaces by calcareous crusts which are thought
to be of algal origin (K. HıLıer 1964, p. 156; K. & H. J. Behr 1976). In the calca-
reous formations of the upper Kimmeridgian the crusts are replaced by stromatolites.
The calcareous crusts are settled by a variety of benthic animals, especially by sessile
worms (serpulids) and forminifera (Nubeculinella). The lower surfaces of the
sponges are overgrown in many cases by serpulids, bryozoans (Berenicea and Stoma-
topora being most frequent), sessile brachiopods (Thecideidae, Craniidae), and other
sessile animals.

During the growth of the sponge-algal bioherms the normal lutitic sedimentation
continued. It was supplemented by the material of the sponges, of the crusts, and of

/ W \
A BT x \
ft FIN
ES
wi N | Na \
@\ı\8 \? url IL | Nusplingen
en U A / Ya j ZT, a a \ S
Ua N ®
we ., ae N y2
E In
St

IN HI
In
0 1000

Fig. 27. The relief of the sponge-algal bioherms at the boundary between the White Jurassic ß
and 7 (boundary Oxfordian/Kimmeridgian) near Nusplingen (southwestern Swabian Alb).
Lines of equal elevation above sea level (in meters). After K. SCHÄDEL in B. ZIEGLER
(1958 a).

34 STUTTGARTER BEITRÄGE ZUR NATURKUNDE Ser.B, Nr. 26

Bamberg®

Regens-
burg

Ingolstadt

Bl sponge facıes

<—— outthrough by meteorite ımpact

ZZ normal facıes

20 40 60 80 100 km

Konstanz Oxfordian:

bımammatum and planula zones

Fig. 28. The extension of the sponge facies in the upper Oxfordian (bimammatum and planula |
zones). Mainly after E. DIETERICH in G. WAGNER (1960), B. v. FREYBERG (1966), R. GyGI!
(1969), and K. HILLER (1964).

other sessile organisms. Therefore in the areas of sponge growth usually the thick-
ness of the sediment is much greater than in the normal facies. Especially in the‘
more marly formations the sponge-algal buildings grew up considerably above the
unsettled sea floor. This primary relief sometimes attained 120 meters. The basins
without sponge-algal growth are named “Schüsseln“.

In southern Germany the first sponge settlements are known from the transver-
sarinm zone of the southwesternmost part of the Swabian Alb (Blumberg). Con-
temporaneous bioherms are widespread in northern Switzerland (Birmenstorf beds).
In the bimammatum zone large parts of the southwestern Swabian Alb and some
regions in the Franconian Alb were covered by sponge-algal bioherms. In the upper-
most Oxfordian and lower Kimmeridgian (planula to hypselocyclum zones) of the
Swabian Alb the distribution of the sponge-algal facies did not change remarkably,
whereas in Franconia a spread of sponge reefs locally occurred already in the upper

ZIEGLER, THE WHITE JURASSIC IN S GERMANY 35

2 sponge facies
domınating
= normal facies

until becker! zone
normal facıes,
replaced by sponge

facıes before
beckeri zone

Tübingen

Upper eudoxus zone
(I41)

sponge facıes
domınatıng

normal facıes
domınatıng

Middle eudoxus zone
(& 3yI)

Er sponge facies
present
SS normal facies

“Sjgmaringen

Upper dıvisum zone

(I ymk )

=S ıgmaringen

SZ = Juttlingen
GE

Fig. 29. The extension of the sponge facies in the Kimmeridgian of the Swabian Alb. Mainly after
K. HıLLer (1964), B. ZIEGLER (1955; 1967), and M. P. GwinNER (1976).

Oxfordian. Starting with the divisum zone, however, a rapid spread of the sponge-
algal bioherms began. They reached their maximum distribution in the upper
endoxus zone. In this period only small areas of normal facies (so-called “Rest-
lücken“) were left. In the latest Kimmeridgian and in the lower Tithonian the
distribution of sponge-algal bioherms was less extensive. It is still unknown when
the sponge growth finally stopped.

The most striking feature in the fauna of the sponge-algal facies is the wealth of
siliceous sponges. A. SCHRAMMEN (1936) noted 136 species, some of which, however,
being possibly only ecological variations. 84 species belong to the Hexactinellida,
this group, however, being more frequent in the Oxfordian and Kimmeridgian than
in the Tithonian. 25 species belong to the rhizomorine Demospongea, which are
represented throughout the stratigraphic column in rather uniform frequency.

36 STUTTGARTER BEITRÄGE ZUR NATURKUNDE Ser. B, Nr. 26

ei sponge facıes
present
= normal facıes

Upper Gravesıa Zone
(„Hangende Bankkalke‘)

sponge facıes
domınatıng
normal facıes

dominatıng

Middle Gravesıa Zone
(Cement marls)

bioclastic and
oolitıc limestones

0 2.8 sponge facıes
0 z u dominatıng
2

normal facıes
domınatıng

Upper becker: and
Lower Gravesıa Zones
(„Liegende Bankkalke”)

Fig. 30. The extension of the sponge facies in the upper White Jurassic of the Swabian Alb. Mainly
after K. HILLER (1964) and M. P. GwinNER (1976).

18 species belong to the tetracladine Demospongea, which are frequent only in the
uppermost Kimmeridgian and in the lower Tithonian.
Although the siliceous sponges are often the most conspicuous fossils they are

not always the most frequent ones. The percentage of individuals represented by |
siliceous sponges varies to a high degree. P. WAGENPLAST (1972, p. 31, 39) mentions |

8 %/o. If the epizoans of the siliceous sponges, such as serpulids, calcareous sponges,
thecideans, and bryozoans, are omitted, about 20 %/o of the individuals are sponges.
This number can be compared rather well with the relationships in the transver-

sarinm zone of northern Switzerland where B. Kress (1967, p. 695) showed the |
sponges to represent 22 °/o of the specimens. On the other hand in other collections

of different localities about 40 ®/o of the individuals are sponges.

ZIEGLER, THE WHITE JURASSIC IN S GERMANY 37

|

in rm nn U = 1 na so ee en 1 100 0 ı 20 ı «0 1 &0
%.of species species

BE Hexactınellida : Tetracladina EEE : Rhizomorina
Other Demosponges

[=]

oe’o

© Heuchstetten
a) ne ©) Gerstetten
Reichenbach
Erkenbrechtsweiler

a
Er - er
sn

OWDiochen
(>) @Hossingen
©) Oberdigisheim

Donau

10 20 30 40 50km

Fig. 31. Some characteristic faunas of siliceous sponges in the White Jurassic of the Swabian Alb.
Note the reduction of Hexactinellida and the greater frequency of Tetracladina in the upper
White Jurassic. After A. SCHRAMMEN (1936) and M. P. GwInNER (1962)

38 STUTTGARTER BEITRÄGE ZUR NATURKUNDE Ser. B, Nr. 26

bıoherm bıoherm bedded bioarenites bedded lutites

Sılıceous sponges >
Crusts and stromatolıtes es Earzreoett
Brachiopods - | ( > — —
Pelecypods

—_——

Isoarca

Ph oladomya DE EEE

other pelecypods

Ammonites Be ee 2 un .0 000 mumz 000}

Foraminıfera

arenaceous foramınıfera

mıilıolids en

rotaliıds
Fig. 32. The ecological distribution of the most frequent fossils in the sponge-algal facies and in |
the normal facies. After G. NITZOPOULOS (1974). |

o Fürstenhöhe near Sigmaringen © Fauna of the normal facıes

—
e Fauna ofthe sponge facıes
o Einödtalbrücke near luttlıngen
aaa oe ee
e Rıngıngen |
1: |

Kol 7 , Dara [ N
e Nusplin en | | |
pu g

| Nucleata

ERRRBER U |

BEZ ——
ß \ Ismenıa and
Trıgonellina
e Nusplingen es je
4 SZ BER | nn
ZZ ER o /rrenberg near Balingen em
Ge and terebratellids
ZZ ——
GES l rhynchonellids

net njie 2 ur Rue ia Pb ee Be eg
[0] 50 100%

Fig. 33. Brachiopod faunas in the Swabian White Jurassic and their composition (according to indi-
viduals) of the most important groups.

39

ZIEGLER, THE WHITE JURASSIC IN S GERMANY

un
TITHONIAN
1 KIMMERIDGIAN

(d3 VIB-c)

n © ee
2 “
EN At:
i ==
Sl! i
NE: S St
1 AL:
S | <= of:
.ofı]) € al |
<i) ® 2
€ << S ||| SE] S
BR EL) Rt
Se Bi] z x | N
ge nl: © si:] 9
st: SW SH S
Sl 01:50
£ a S) S)
Ö [N
[®) © Q Q z z
© D < S
Sci Si 5
NR u W
d i = Q x x
: Fi) < < 5
i fr (2) © &
sen eo «I =; .O
— |® wo
A E
jo [2 S

|
[e)
|
®
|

Sauserbrunnen, uppermost bımammatum zo

Barenthal, hypselocyclum zone

Nusplingen, platynota zone

8
t bımammatum zone

N
|

l

Barenthal, platynota zone

mmatum zone

KIMMERIDGIAN
OXFORDIAN

0
Barenthal, uppermos

Häfnershalde, bima

Is

Is

„8 Er
Bärenthal, bimammatum zone |

Ü
Sa Mar:

Ü
ressa Mar

© fauna of the normal facıes

„® fauna of the sponge facıes

Yo

Irrenberg, ımpres
Reichenbach, ımp

n

Blumberg, transversarıum zone

50 :
| phylloceratids
| Amoeboceras

30

Haploceratacea

0 I aspıdoceratids

perisphinctids

0

Fig. 34. Ammonite faunas in the Swabian White Jurassic and their composition (according to indi-
viduals) of the major ammonite groups.

Owing to their considerable sizes the siliceous sponges sometimes form more
than 50 °/o of the sediment. Especially in the more marly formations they often are
the constructive element of the rock. In the more calcareous formations, however,
they may occur rather scattered (compare R. Meyer 1975, p. 158).

The brachiopods are another characteristic group of the sponge-algal facies.
They represent often more than 20 °/o of the specimens. The most abundant genera

40 STUTTGARTER BEITRÄGE ZUR NATURKUNDE Ser. B, Nr. 26

EJ Perisphinctids
Aspıdoceratids
MM Amoeboceras

| Haploceratacea

Salmendingen

Unterhausen

Fig. 35. The composition (according to individuals) of two ammonite faunas of the major ammonite
groups. White Jurassic 61 (lower acanthicum zone) of the central Swabian Alb.
Salmendingen: Section with sponge-algal limestones within a region of predominant sponge
facies.

Unterhausen: Section with some sponge-algal limestones within a region of predominant
normal facies.

are Lacunosella (especially in the lower part of the divisum zone where this genus
sometimes forms the majority of the organisms in small bioherms) and Loboidothyris.
Terebratulina and other small terebratulids and terebratellids are frequent only in
certain parts of the sponge-algal facies (p. 43). Craniids and thecideans occur as
epizoans especially on the sponges.

In life the ammonites did not belong to the community of the sponge-algal bio-
herms. However, they are deposited rather frequent in the sponge-algal facies and
it seems that they lived near the sea floor. Sometimes they are represented by more
than 60 %o of the specimens, in other cases they are much more rare. Some genera
or species (e. g. Amoeboceras, Creniceras dentatum, Glochiceras canale) are much
more abundant near or in the sponge-algal facies than in the normal facies. The
relative abundance of genus groups is highly variable. It seems that in general the
Haplocerataceae are more frequent in marginal parts of the sponge-algal bioherms
than in the normal facies but that in the central parts of the reefs often the Peri-
sphinctaceae become more frequent. In addition differences during time can be
shown. Therefore no general rule can be established.

Macroscopical Echinodermata are found in the sponge-algal bioherms rather
scattered, being mostly represented by regular echinids and their spines. Pelecypods

41

ZIEGLER, THE WHITE JURASSIC IN S GERMANY
mm ostracods Ba echinoderms ca other microfossils

zes foramınıfers
B
®

®
u)

! 2 5)

Hass 100%

1 un:

(0) 50
Fig. 36. The microfauna of marly sponge-algal sediments in the Swabian White Jurassic. After P.

WAGENPLAST (1972).
A: Percentage of individuals in the most important groups.
B: Number of individuals (in thousands) in samples of 110 g.

——— P | : Reophax
= elle wlan ©
gglutinatıng
= = j nere
go
m A ] Be
gg Spirillina
ss
| other calcareous
n rn En Ts == foramınıfers
5 100%

er ..ä— —
m l
. 0 0
Fig. 37. Percentage of individuals of the most important foraminifera in some samples from marly

sponge-algal sediments in the Swabian White Jurassic. After P. WAGENPLAST (1972).

42 STUTTGARTER BEITRÄGE ZUR NATURKUNDE Ser. B, Nr. 26

% of arenaceous and miliolid foraminıfera
10

Valvulina lobata E.& I.SEIBOLD

/m

Fig. 38. The arenaceous foraminifer Valvulina lobata E. & I. SEIBOLD and its restriction to sponge-
algal sediments (stippled). After E. & I. SEIBOLD (1960). |

are rare; their majority consists of the valves of fixosessile spondylids which grew
on sponges.

The microfauna of the sponge-algal bioherms is dominated by foraminifera. As
could be shown by E. & I. SerwoLp (1960, p. 395) a variety of species and genera is
much more frequent in the sponge-algal facies than in the normal facies. The most
important companions of the sponge-algal reefs are Spirillina, Rheophax, Lenticulina,
and Paalzowella (P. WAGENPLAST 1972, p. 14). A quite peculiar microfauna occurs
in the channel-systems of the siliceous sponges. However, owing to the mode of
preparation, only the agglutinating foraminifera are known. Subbdelloidina,
Trochammina, Thurammina, and Tolypammina are the most frequent genera
(P. WAGENPLAST 1972, p. 20).

Östracods are rare. The echinoderms are the second major group in the micro- !
fossils. Most frequent are the skeletal elements of ophiuroids, followed by those of |
crinoids and asteroids.

Parts of the sponge-algal facies, especially those with high carbonate content, |
were altered during diagenesis. Thus large areas now are covered by dolomites and
saccharoidal limestones which are interpreted as the result of dedolomitization (H.
B. Lang 1964). At some localities in the Swabian Alb and widespread in the Fran-
conian Alb the dolomites are not restricted to the bioherms but have penetrated
into the normal facies, too (R. MEYER 1972; 1974).

ZIEGLER, THE WHITE JURASSIC IN S GERMANY 43
Goamkiche Kochen Daceıres

In the marly formations of the upper Oxfordian and of the lower Kimmeridgian
especially (but by no means exclusively) marginal parts of the sponge-algal bioherms
show quite peculiar relationships. They are crowded with small, sometimes dwarfed
fossils. This facies, which is named the Lochen facies after the Lochen beds of the
bimammatum zone, is intimately linked with the common sponge-algal facies. No
sharp boundary can be drawn.

The most striking feature of the Lochen facies is the high percentage of small
individuals in the fauna. Even in the siliceous sponges many small specimens occur,
belonging mostly to Sporadopyle or Trochobolus. The brachiopods are represented
to a large degree by genera and species otherwise missing. Characteristic forms are
Nucleata, Zittelina, Trigonellina, Ismenia, Terebratulina, and other small Terebra-
tulida and Terebratellida. Normal sized Lacunosella and Loboidothyris are present,
too. It appears that the majority of the small brachiopods is fully grown (cf. K. VoceL
1959, p. 124).

Ammonites are often abundant. Although the bulk of the specimens seems to
be adult, juveniles are present, too. Some ammonite species and genera are much
more frequent in the Lochen facies than elsewhere in the Swabian Alb (e. g. Amoe-
boceras, Epipeltoceras). Others apparently are totally restricted to this facies (e. g.
“Enaspidoceras“ bidentosum). The most characteristic species in the Lochen facies
of the bimammatum zone are Taramelliceras lochense, T. pichleri, and Glochiceras
canale.

In the Echinodermata small representatives of crinoids and echinids are common.
The most frequent crinoids are Balanocrinus and Eugeniacrinites. Characteristic
echinids are cidaroids and Pseudodiadema. Whether the small echinids are dwarfed
specimens or juveniles is unknown. As in the brachiopods the small species are
accompanied by normal sized cidaroids. In addition to crinoids and echinids skeletal
plates of asteroids occur.

6.3. Basins with calcareous shales

In the topmost Kimmeridgian (uppermost beckeri zone) in some deep basins
(“Schüsseln“) between the elevated culminations of the sponge-algal bioherms the
deposition of calcareous shales took place. The original thickness of the sediment
was much higher as it appears now; during diagenesis the rocks were compressed to
about one tenth of the former state. Fossils are very rare but the extensive quarrying
has yealded a very interesting fauna and flora in a considerable number of specimens.
Apparently the water near the sea floor in the basins was very poor in oxygen.
Therefore benthic life was extremely scarce, but allochthonous, mostly nectic or
planctic fossils were preserved extraordinary well.

In the southwestern part of the Swabian Alb basins with deposition of calcareous
shales existed in the uppermost beckeri and the lowermost Gravesia zones. Best
known is the basin of Nusplingen which yealded ammonites, crustaceans, fishes,
even some reptiles, and plants. However, the fossils are very scarce. Other basins
existed near Kolbingen and Tiergarten (H. TEMMLER 1964).

44 STUTTGARTER BEITRÄGE ZUR NATURKUNDE Ser. B, Nr. 26

7 Reef facıes — Basın facıes 3 Maın distribution of resediments

Altmühl N
Weißenburg ®

Ingolstadt

Regensburg
ns

„NEingen

Donauwörth
D: Daiting M: Mörnsheim
E: Eıchstatt Pa: Paınten
J: Jachenhausen Pf: Pfalzpaınt
K: Kelheim S: Solnhofen
DM him L: Langenaltheim Z: Zandt

Fig. 39. The distribution of the basin facies (mainly lithographic calcareous shales) within the upper
Solnhofen formation (lower Tithonian) in the southern Franconian Alb. After B. v. FrREY-
BERG (1968).

By far more important are the calcareous shales in the southern Franconian Alb.
They are somewhat younger and belong mainly to the Gravesia zone. However,
deposition of the calcareous shales started in the Torleite beds (beckeri zone) and
continued locally until the Rennertshofen formation (vimineus zone). The most fa-
mous outcrops are situated in the region of Solnhofen and Moernsheim, in the sur-
roundings of Eichstätt, and near Pfalzpaint, Zandt, Daiting, and Painten. The beds
are known as the Solnhofen lithographic shales (cf. K. W. BARTHEL 1970; 1972).

The most frequent fossils in these shales are the free swimming crinoid Sacco-
coma and the ammonite genus Glochiceras. Both are rather common findings. All
other fossils are rare. However, due to the extensive exploitation of the rocks now
large materials are known. Best represented are small fishes (especially Leptolepis)
and decapod crustaceans.

In total about 700 species of macrofossils have been described from the Soln-
hofen shales, the taxonomic validity of some being disputable, however. Many
species are represented only by one or few specimens. The taxonomic diversity is
largest in insects (about 180 species), followed by fishes (about 150 species),
crustaceans (about 60 species), and reptiles (about 60 species). For literature on
the fauna and flora of the Solnhofen shales see OÖ. Kunn (1961; 1963).

The most outstanding findings in the Solnhofen lithographic shales are the five
skeletons of Archaeopteryx. Whereas these birds were fossilized far outside their
biotope, the pterosaurians apparently lived near or on the sea. They are represented
by several genera belonging to the long-tailed Rhamphorhynchoidea and to the
short-tailed Pterodactyloidea as well. Some specimens still show the contents of the

ZIEGLER, THE WHITE JURASSIC IN S GERMANY 45

worms__coelenterates sponges_ plants_ bırds

al:
pelecypods h reptiles
ammonıtes— HEN ii
other cephalopods—} OT
Zeereai un RD
rn
SÜSSE —— ——= fıshes

echınoderms
bryozoans
brachıopods

Iotal: about 660 species other arthropods

The most frequent groups are underlıned

Fig. 40. The composition (according to species) of the macrofauna of the calcareous shales of the
Altmühltal group (lower Tithonian) in the southern Franconian Alb. After O. Kunn (1963).

stomach (remains of fishes and crinoids). The aquatic saurians such as ichthyosaurians,
plesiosaurians, turtles, and crocodilians are very rare. More frequent are represen-
tatives of the Rhynchocephalia, especially Homoeosaurus, which occurs preferably
in the easternmost localities. Homoeosaurus apparently had amphibic life habits.
True terrestrial reptiles occur with but a unique specimen (Compsognathus).

Fishes are known in all states of preservation. A biostratinomical survey of
this group reveals that in many cases drifting dead bodies were disintegrated. Parts
fell down to the sea floor and were embedded isolatedly. On the other hand, decay
of dead bodies on the sea floor is proven, too. Finally, in more exceptional cases
complete skeletons are preserved. Apparently all these processes went on under
permanent covering by sea water. An occasional draining of the sedimentary basin
as it was postulated by ©. AseL (1927, p. 580) and F. X. Mayr (1967) is not
proven (K. W. BArTHEL 1970; 1972).

Soft-bodied animals are preserved in the Solnhofen shales very rarely but in an
extremely good manner. Jelly-fishes, worms, and cuttle-fishes are known with
excellent specimens. Especially the study of imprints of the arms of cuttle-fishes
gives important informations. Dead animals drifted in the water of the Solnhofen
basin. When they sunk to the sea floor sometimes they came down first with their

46 STUTTGARTER BEITRÄGE ZUR NATURKUNDE Ser. B, Nr. 26

arms and left regular eight-rayed rosettes. Then they canted over and were embedded
_ immediately beside these imprints. Evidently the water movement was insignificant.
Perhaps this caused poverty in oxygene which may be the reason for the good
preservation of the fossils.

However, in some parts of the sedimentary basins, especially in the eastern out-
crops, considerable water movements have existed at least sometimes. This is proven
by the findings of marks produced by rolling empty ammonite shells (A. SEILACHER
1963). Thus the genesis of the Solnhofen shales is by no means exactly known.

6.4. Ihe shallow water facies

During the Kimmeridgian the development of sponge-algal bioherms had lead to
a considerable submarine relief (p. 34). For long times the subsidence of the sea
floor seems to have equalled the growth of the bioherms. As it is indicated by the
autochthonous faunas the depth of the sea appears to have never been less than
about 70 to 100 m even on the summits of the bioherms.

However, in the late Kimmeridgian signs of shallowing of the sea set in. It is
not quite certain whether this shallowing is the result of the continuing growth of
the bioherms or of some epirogenetic movements. In the Swabian Alb several sub-
marine slumps, breccias, and resediments are known from the “Liegende Bankkalke“.
Similar phenomena are widespread in the lower Tithonian of the southern Franco-

nian Alb.

When culminations of the sponge-algal bioherms grew up to a position near the
sea-level (or when they were uplifted to this position) they were overgrown by a
fauna of reef corals and their allies. The first coral growth took place in the sur-
roundings of Kelheim in the southeasternmost Franconian Alb. There it is of upper
Kimmeridgian age (basal beckeri zone, perhaps even eudoxus zone). Other coral
faunas in the southern Franconian Alb and in the eastern parts of the Swabian Alb

|
ı
are younger (lower Tithonian: Gravesia zone). |
|

Most famous is the locality of Nattheim (eastern Swabian Alb). The revision of
the corals of the Swabian Alb by ©. F. Geyer (1954) showed that at Nattheim ı
predominantly reef detritus is present. The same is likely for most other localities.
In some places, however, the fauna is more or less autochthonous and the former
bioherms and biostromes are preserved rather well (e. g. Arnegg and Laisacker).

The coral fauna of the lower Tithonian in the Swabian Alb is extremely rich in
species. ©. F. GEYER (1954, p. 209) records about 150 species, some of which being !
restricted to only one or a few localities. According to ©. F. Geyer (1954, p. 209), |
in Kelheim only 85 species are present. They are found in a restricted area with only |
few outcrops, however.

The reef corals are accompanied by a great variety of other shallow wat
fossils. In the Swabian Alb, where about 130 species are recorded (O. F. GEYER |
1953a, p. 137), especially thick-shelled pelecypods and gastropods are well represen- |
ted. The majority of the pelecypods belongs to the Pteriomorpha (e.g. Trichites, |
Arctostrea, limids, pectinids). The most important gastropods are pleurotomariids )
and nerineids.. Ammonites are extremely rare. In addition to the molluscs a rich |

ZIEGLER, THE WHITE JURASSIC IN S GERMANY 47

e|

SL Sınabronn Kelheim

Sirchingen Pappelau

Sandharlanden (©)

2 Demling
LLIYS L er LaisackerO, -ORied OGrossmehring
Guss@®nstadt „ONattheim
\ O Gerstetten

Sınabronn
. Donnstetteno | O Oberstotzıngen
Sırchingen® [6) Bermaringen
Wittlingen 6, rnegg 20
- Pappelau

10
number of species

Ä Donau
a — predominantly massıve corals
de IT predominantly phaceloıd and solitary corals

2 0 20 40 60 80 00km - Fe predomınantly folıose and dendroıd corals

Fig. 41. The composition (according to individuals) of major ecological groups and the diversity of
some coral faunas of the upper Malm of southern Germany. After ©. F. GEYER (1954).

fauna of calcareous sponges, brachiopods (e. g. Septaliphoria, Juralina, Cheirothyris),
and echinodermata (especially Millericrinus and cidaroids) is present.

In the southern Franconian Alb the composition of the mollusc fauna seems to
differ somewhat from that in the Swabian Alb. Whereas Diceras is very rare in the
Swabian Alb (©. F. Geyer 1953 b) it occurs frequently in Franconia (e.g.in Kel-
heim and Großmehring). Therefore the recifal limestones of Kelheim are named the
‚“Diceras-Kalk“. Moreover heterodont pelecypods are well represented in the
southern Franconian Alb but are rare in Swabia. However, perhaps this is due to
differences in preservation or even in collecting.

6.5. The Neuburg formation

The recifal and related sequence of the lower Tithonian is followed by regularly
bedded limestones which are preserved only in a very restricted area near Neuburg an
der Donau. Consequently this formation is named the Neuburg formation. It is proven
to be of middle Tithonian age, the topmost parts belonging to the upper Tithonian.

48 STUTTGARTER BEITRÄGE ZUR NATURKUNDE Ser. B, Nr. 26

—J ]specıes

Species

—]] genera

| species

- TE ————J] species
1] species
| specimens
MINE ———J]genera
|
AALEN ————ÜU genera

ı

SwabıanAlb Bermaringen Laisacker Grossmehring Kelheim
(‚normal facıes‘) Oberstotzingen

ee >

a,

c-
=

©

TE Bu:

-Kelheım

B Oberstolzingen
Bermaringen
10

5
number of species and genera

IR Er Palaeoheterodonta and Veneroida

02020 ram | Iozeuuz:
[_ (GE ci EEE om]

Fig. 42. The composition of major groups and the diversity of some pelecypod faunas of the upper
Malm of southern Germany. Swabian Alb after Tu. ENGEL (1908). Bermaringen and Ober-
stotzingen after ©. F. GEYER (1953 a). Laisacker, Großmehring, and Kelheim after S.-A.
YAMANI (1973; 1975; 1976), and S.-A. YAMANI & G. SCHAIRER (1975).

ZIEGLER, THE WHITE TURASSIC IN S GERMANY 49

The lower and middle parts of the Neuburg formation (Unterhausen beds and lo-
wer Oberhausen beds) yeald a rich fauna of ammonites (Th. ScHneip 1915; K.W.Bar-
THEL 1962; K. W. BAarTHEL & J. R. Geyssant 1973), pelecypods (P. WELLNHOFER
1964), and gastropods (V. JAnıckE 1966). Corals and especially sponges are recorded
only with few specimens (D. HerMm 1966; W. WAGNER 1965). Frequent microfossils
are foraminifers (J. Tu. Groiss 1967; J. Tu. Groıss & B. WınTer 1967), ostracods
being present, too, but badly preserved and of poor diversity (H. J. OErTLI 1965).

The ammonites are dominated by perisphinctids. The most frequent pelecypods
are Grammatodon, Pinna, Exogyra, Rollierella, and Loripes. Gastropods are much
less frequent than pelecypods, being represented especially by Amberleya and Proce-
rithella. In the foraminifers a preponderance of the Rotaliina, especially of the
Nodosariacea, over the Textularida is documented. Of special interest is the presence
of Psendocyclammina.

In the upper part of the Neuburg formation (upper Oberhausen beds) once more
siens of shallowing of the sea are obvious. Ammonites are missing. Pelecypods and
gastropods are well represented. Especially the presence of certain pelecypods
(Eocallista, Neomiodon, Eomiodon, Thracia, Unio) indicates reduced salinity. How-
ever, in the uppermost beds genera as Nuculoma, Inoperna, Lima, and Myophorella
point to normal salinity. The most significant foraminifera are large agglutinating
forms (Anchispirocyclina and Pseudocyclammina) which are accompanied especially
by Ammobaculites, miliolids, and Trocholina. In addition a variety of algae is pre-
sent (K. W. BARTHEL 1969).

7. Literature

Works containing comprehensive references are marked by an asterisk (x)

ABEL, ©. (1927): Lebensbilder aus der Tierwelt der Vorzeit. 2nd ed., VIII+714 pp., 2 pls., 551 figs.;
Jena (G. Fischer).

ALDINGER, H. (1945): Zur Stratigraphie des Weißen Jura ö in Württemberg. — Jber. Mitt. ober-
rhein. geol. Ver., n. F. 31 (1942), p. 111—152, 3 figs., 1 tab.; Stuttgart.

AMMon, L. von (1875): Die Jura-Ablagerungen zwischen Regensburg und Passau. — Abh. zool.-
mineral. Ver. Regensburg, 10, p. III-X, 1-200, pl. 1-4; München.

BANTZ, U. (1970): Der Fossilinhalt des Treuchtlinger Marmors (Mittleres Unter-Kimmeridge der Süd-
lichen Frankenalb). — Erlanger geol. Abh., 82, 86 pp., 6 pls. 6 figs.; Erlangen.

50 STUTTGARTER BEITRÄGE ZUR NATURKUNDE Ser. B, Nr. 26

BARTHEL, K. W. (1962): Zur Ammonitenfauna und Stratigraphie der Neuburger Bankkalke. — Abh.
Bayer. Akad. Wiss., math.-naturwiss. Kl., n. F. 105, 30 pp., 5 pls., 4 figs.; München.
— (1969): Die obertithonische, regressive Flachwasser-Phase der Neuburger Folge in Bayern. —
Abh. Bayer. Akad. Wiss., math.-naturwiss. Kl., n. F. 142, 174 pp., 14 pls., 39 figs.;
München.
— (1970): On the deposition of the Solnhofen lithographic limestone (Lower Tithonian, Bava-
ria, Germany). — N. Jb. Geol. Paläont., Abh., 135, p. 1-18, pl. 14, 2 figs. 1 tab.;
Stuttgart.
— (1972): The genesis of the Solnhofen lithographic limestone (Low. Tithonian): further data
and comments. — N. Jb. Geol. Paläont. Mh., 1972/3, p. 133—145, 4 figs.; Stuttgart.
BARTHEL, K. W. & GEYySsSANT, J. R. (1973): Additional Tethydian ammonites from the lower
Neuburg formation (Middle Tithonian, Bavaria). — N. Jb. Geol. Paläont., Mh., 1973/1,
p. 18-36, 5 figs.; Stuttgart.

BAuscH, W. M. (1971): Tonmineralprovinzen im europäischen Malm. — Ann. Inst. geol. publ.
Hungar., 54/2, p. 333—334; Budapest.

BEHR, K. & H.-J. (1976): Cyanophyten aus oberjurassischen Algen-Schwamm-Riffen. — Lethaia, 9,
p. 283—292, 8 figs.; Oslo.

BERCKHEMER, F. (1922): Beschreibung wenig bekannter und neuer Ammonitenformen aus dem
Oberen Weißen Jura Württembergs. — Jh. Ver. vaterl. Naturkde. Württ., 78, p. 68-80, 1 pl.,
1 fig.; Stuttgart.

BERCKHEMER, F. & HÖLDER, H. (1959): Ammoniten aus dem Oberen Weißen Jura Süddeutsch-
lands. — Beih. geol. Jb., 35, 135 pp., 27 pls., 89 figs.; Hannover.

BEURER, M. (1963): Die Geologie des Blattes Oberkochen (Nr. 7226) 1:25 000 (Ostalb). — Arb.
geol.-paläont. Inst. T. H. Stuttgart, n. F. 36, 123 pp., 5 pls., 5 figs.; Stuttgart.

CALLOMON, J. H. (1964): Notes on the Callovian and Oxfordian Stages. — Coll. Jurass. Luxembourg
1962; C. r. Mem. Inst. grand ducal, Sect. Sci. natur., phys., math., p. 269-291; Luxembourg.

DIETERICH, E. (1940): Stratigraphie und Ammonitenfauna des Weißen Jura # in Württemberg. —
Jh. Ver. vaterl. Naturkde. Württ., 96, p. 1-40, pl. 1-2, 6 figs.; Stuttgart.

ELWERT, D. (1963): Die Geologie des Blattes Ebingen (Nr. 7720) 1:25 000 (Schwäbische Alb). —
Arb. geol.-paläont. Inst. T.H. Stuttgart, n. F. 37, 50 pp., 4 pls., 1 fig., 1 tab.; Stuttgart.

ENGEL, TH. (1908): Geognostischer Wegweiser durch Württemberg, 3rd ed., 645 pp., 6 pls., 270 figs.,
1 map; Stuttgart (Schweizerbart).

x FLÜGEL, E. (edit.) (1975): International Symposium on Fossil Algae. Guide Book. 228 pp., 53
figs.; Erlangen (Inst. Paläont. Univ.).

FLÜGEL, E. & FRANZ, H. E. (1967): Elektronenmikroskopischer Nachweis von Coccolithen im Soln-
hofener Plattenkalk (Ober-Jura). — N. Jb. Geol. Paläont., Abh., 127, p. 245—263, pl. 24—26,
fies tabs: Stuttgart:

FRAAS, ©. (1882): Geognostische Beschreibung von Württemberg, Baden und Hohenzollern. 218 pp.;
Stuttgart (Schweizerbart).

FREYBERG, B. VON (1966): Der Faziesverband im Unteren Malm Frankens. Ergebnisse der Stro-
matometrie. — Erlanger geol. Abh., 62, p. 1-92, pl. 1-8, fig. 1—16, tab. 1-3; Erlangen.
— (1968): Übersicht über den Malm der Aitmühl-Alb. — Erlanger geol. Abh., 70, 40 pp., 4 pls.,
5 figs.; Erlangen.
* — (1974): Das geologische Schrifttum über Nordost-Bayern (1476-1965). Teil I. Bibliographie.
— Geologica Bavarica, 70, 467 pp., 1 fig.; München.

FRITZ, G. K. (1958): Schwammstotzen, Tuberolithe und Schuttbreccien im Weißen Jura der Schwä-
bischen Alb. Eine vergleichende petrogenetische Untersuchung. — Arb. geol.-paläont. Inst.
T. H. Stuttgart, n. F. 13, 118 pp., 5 pls., 24 figs.; Stuttgart.

GEBERT, H. (1964): Die Geologie des Blattes Meßstetten (Nr. 7819) 1:25 000 (Schwäbische Alb). —
Arb. geol.-paläont. Inst. T. H. Stuttgart, n. F. 45, 93 pp., 6 pls., 6 figs., 2 tabs.; Stuttgart.

GEYER, OÖ. F. (1953): Die Fauna der oolithischen Trümmerkalke des oberen Malm in Württemberg
und ihre Beziehungen zur koralligenen Fazies des Tithon. — N. Jb. Geol. Paläont., Mh.,
1953/3, p. 130—140, 2 tabs.; Stuttgart. — |1953a]

ZIEGLER, THE WHITE JURASSIC IN S GERMANY 51

— (1953): Über Diceras speciosum (MÜNSTER) im Weißen Jura von Württemberg. — Paläont.
Z., 27, p. 208—211, pl. 13; Stuttgart. — [1953b]

— (1954): Die oberjurassische Korallenfauna von Württemberg. — Palaeontographica, A, 104,
p. 121—220, pl. 9—16, 2 tabs.; Stuttgart.

— (1961): Beiträge zur Stratigraphie und Ammonitenfauna des Weißen Jura y (Unteres Unter-
kimeridgium) in Württemberg. — Jh. Ver. vaterl. Naturkde. Württ., 116, p. 84—113, 3 figs.,
5 tabs.; Stuttgart. — [1961a]

— (1961): Monographie der Perisphinctidae des unteren Unterkimeridgium (Weißer Jura y,
Badenerschichten) im süddeutschen Jura. — Palaeontographica, A, 117, p. 1—157, pl. 1—22,
157 figs., 107 tabs.; Stuttgart. — [1961b]

GEYER, O. F. & GWINNER, M. P. (1961): Führer zu den Exkursionen anläßlich der 82. Tagung des
Oberrheinischen Geologischen Vereins in Ulm vom 4. bis 8. April 1961. — Arb. geol.
paläont. Inst. T. H. Stuttgart, n. F. 30, 51 pp., 16 figs., 2 tabs., 1 suppl.; Stuttgart.

— Der Schwäbische Jura. — Samml. geol. Führer, 40, 452 pp., 46 figs., 4 suppl.; Berlin.

GLASHOFF, H. (1964): Ostrakoden-Faunen und Paläogeographie im Oxford NW-Europas. — Paläont.
Z., 38, p. 28—65, pl. 4—5, 3 figs. 4 tabs.; Stuttgart.

Groıss, J. TH. (1966): Eine Foraminiferen-Fauna aus Ätzrückständen von Massenkalken des süd-
deutschen Ober-Malm. — Geol. Bl. NO-Bayern, 16, p. 39—49, 1 fig.; Erlangen. — [1966a]

— (1966): Das Problem der Malm Alpha/Beta-Grenze in mikropaläontologischer Sicht. — Er-
langer geol. Abh., 62, p. 92—104, fig. 17—22, tab. 4-5; Erlangen. — [1966b]

— (1967): Foraminiferen-Faunen aus den Neuburger Bankkalken. — Erlanger geol. Abh., 66,
p- 3—74, pl. 1—4, 6 figs.; Erlangen. — [1967a]

— (1967): Mikropaläontologische Untersuchung der Solnhofener Schichten im Gebiet um Eich-
stätt (Südliche Frankenalb). — Erlanger geol. Abh., 66, p. 75—96, pl. 5, 3 figs.; Erlangen. —
[1967b]

— (1970): Feinstratigraphische, ökologische und zoogeographische Untersuchungen der Forami-
niferen-Faunen im Oxford der Franken-Alb. — Erlanger geol. Abh., 81, 83 pp., 9 figs.,
2 tabs.; Erlangen.

GroIsS, J. TH. & WINTER, B. (1967): Das Vorkommen von Pseudocyclammina und Lituola (Foram.)
in den Neuburger Bankkalken (Mittel-Tithon). — Geol. Bl. NO-Bayern, 17, p. 109-127,
pl. 5—6, 6 figs.; Erlangen.

GWINNER, M. P. (1962): Geologie des Weißen Jura der Albhochfläche (Württemberg). — N. Jb.
Geol. Paläont., Abh., 115, p. 137—221, pl. 10—13, 22 figs., 1 tab.; Stuttgart.

* — Origin of the Upper Jurassic Limestones of the Swabian Alb (Southwest Germany). — Contr.
Sedimentology, 5, 75 pp., 66 figs., 6 tabs.; Stuttgart.

GyGI, R. (1966): Über das zeitliche Verhältnis zwischen der transversarium-Zone in der Schweiz
und der plicatilis-Zone in England (unt. Malm, Jura). — Eclogae geol. Helvet., 59, p. 935—
942, pl. 14, 1 fig.; Basel.

— (1969): Zur Stratigraphie der Oxford-Stufe (oberes Jura-System) der Nordschweiz und des
süddeutschen Grenzgebietes. — Beitr. geol. Karte Schweiz, n. F. 136, 123 pp., 19 pls., 11
figs., 9 tabs.; Bern.

Haag, H. W. (1960): Die Geologie des Blattes Zwiefalten (Nr. 7722) 1:25 000 (Stratigraphie und

| Tektonik der Zwiefalter Alb). — Arb. geol.-paläont. Inst. T. H. Stuttgart, n. F. 28, 121 pp.,
2 pls., 6 figs.; Stuttgart.

Hann, W. & KOERNER, U. (1971): Die Aufschlüsse im oberen Dogger (Bathonium-Callovium) im
Albstollen der Bodenseewasserversorgung unter der Zollernalb (SW-Deutschland). — Jh. geol.
Landesamt Baden-Württemberg, 13, p. 123—144, pl. 10-12, 3 figs.; Freiburg im Breisgau.

HAFNER, G. (1969): Die Geologie des Blattes Nendingen (Nr. 7929) 1:25 000 (Schwäbische Alb). —
Arb. geol.-paläont. Inst. Univ. Stuttgart, n. F. 58, 246 pp., 12 pls., 20 figs.; Stuttgart.

HAUERSTEIN, G. (1966): Perisphinctes (Arisphinctes) aus der Plicatilis-Zone (Mittel-Oxfordium)
von Blumberg/Südbaden (Taxionomie; Stratigraphie). — Thesis Univ. München, 112 pp.,

| 5 pls., 19 figs., 7 tabs.; München.

HENNIG, E. (1943): Der Schwäbische Obere Weißjura, eine Zusammenschau. — N. Jb. Mineral,
Geol. Paläont., Mh., 1943, B, p. 81—100; Stuttgart.

HERM, D. (1966): Korallen aus den Neuburger Bankkalken (Mittel-Tithon) von Neuburg an der
Donau. — Mitt. Bayer. Staatssamml. Paläont. hist. Geol., 6, p. 21-32, 5 figs.; München.

52 STUTTGARTER BEITRÄGE ZUR NATURKUNDE Ser. B, Nr. 26

Hrtter, K. (1964): Über die Bank- und Schwammfazies des Weißen Jura der Schwäbischen Alb
(Württemberg). — Arb. geol. paläont. Inst. T. H. Stuttgart, n. F. 40, 190+ XIII pp., 26 pls.,
38 figs., 4 tabs.; Stuttgart,

HöLDer, H. (1964): Jura. 603 pp., 158 figs., 43 tabs.; Stuttgart (Enke).

JANICKE, V. (1966): Die Gastropoden und Scaphopoden der Neuburger Bankkalke (Mittel-Tithon).—
Palaeontographica, A, 126, p. 35—69, pl. 11—13, 2 tabs.; Stuttgart.

Keurr, H. (1976): Der Solnhofener Plattenkalk — Ein neues Modell seiner Entstehung. — Jmitt.
naturhist. Ges. Nürnberg, 1975, p. 19-36, 16 figs.; Nürnberg.

KLEMENT, K. W. (1960): Dinoflagellaten und Hystrichosphaerideen aus dem unteren und mittleren
Malm Südwestdeutschlands. — Palaeontographica, A, 114, p. 1-104, pl. 1-10, 37 figs.,
1 tab.; Stuttgart.

KNOBLAUCH, G. (1963): Sedimentpetrographische und geochemische Untersuchungen an Weißjura-
kalken der geschichteten Fazies im Gebiet von Urach und Neuffen. — Thesis Univ. Tübingen,
105 pp., 9 figs.; Tübingen.

KNOBLICH, K. (1963): Die Geologie des Blattes Elchingen (Nr. 7227) 1:25 000 (Schwäbische Alb).
— Arb. geol.-paläont. Inst. T. H. Stuttgart, n. F. 39, 49 pp., 9 figs.; Stuttgart.

KOERNER, U. (1963): Beiträge zur Stratigraphie und Ammonitenfauna der Weißjura-a/ß-Grenze
(Oberoxford) auf der westlichen Schwäbischen Alb. — Jh. geol. Landesamt Baden-Württem-
berg, 6, p. 337—394, pl. 22—32, fig. 39—73; Freiburg im Breisgau.

Kregs, B. (1967): Zwei Steneosaurus-Wirbel aus den Birmenstorfer Schichten (Ober-Oxford) vom
„Weissen Graben“ bei Möntal (Kt. Aargau). — Eclogae geol. Helvet., 60, p. 689-695,
2 figs.; Basel.

*» Kunn, ©. (1961): Die Tier- und Pflanzenwelt des Solnhofener Schiefers. Mit vollständigem
Arten- und Schriftenverzeichnis. — Geologica Bavarica, 48, 68 pp., 1 fig.; München.

— (1963): Die Tierwelt des Solnhofener Schiefers. — Neue Brehm Bücherei, 318, 36 pp.,
115 figs.; Wittenberg. |

Lang, H. B. (1964): Dolomit und zuckerkörniger Kalk im Weißen Jura der mittleren Schwäbischen
Alb (Württemberg). — N. Jb. Geol. Paläont., Abh., 120, p. 253—299, pl. 18—22, 18 figs.;
Stuttgart.

LirticH, W. (1962): Die Geologie der Blätter Mehrstetten und Schelklingen (Nr. 7623 und Nr.
7624) 1:25 000 (Schwäbische Alb). — Arb. geol.-paläont. Inst. T. H. Stuttgart, n. F. 34,
111 pp., 6 pls., 8 figs.; Stuttgart.

MAYR, F. X. (1967): Paläobiologie und Stratinomie der Plattenkalke der Altmühlalb. — Erlanger
geol. Abh., 67, 40 pp., 16 pls., 8 figs.; Erlangen.

MEYER, R. K. F. (1972): Stratigraphie und Fazies des Frankendolomits (Malm). 1. Teil: Nördliche '

Frankenalb. — Erlanger geol. Abh., 91, 28 pp., 5 pl., 25 figs.; Erlangen.

— (1974): Stratigraphie und Fazies des Frankendolomits (Malm). 2. Teil: Mittlere Franken- -
alb. — Erlanger geol. Abh., 96, 34 pp., 3 pls., 12 figs.; Erlangen.

— (1975): Mikrofazielle Untersuchungen in Schwamm-Biohermen und -Biostromen des Malm ı
Epsilon (Ober-Kimmeridge) und obersten Malm Delta der Frankenalb. — Geol. Bl. NO-Bayern,
25, p. 149—177, 14 figs., 2 tabs.; Erlangen.

— (1977): Stratigraphie und Fazies des Frankendolomits und der Massenkalke (Malm). 3. Teil:
Südliche Frankenalb. — Erlanger geol. Abh., 104, 40 pp., 50 pls., 10 figs; Erlangen.

NITZOPOULOS, G. (1974): Faunistisch-ökologische, stratigraphische und sedimentologische Untersu-
chungen am Schwammstotzen-Komplex bei Spielberg am Hahnenkamm (Ob. Oxfordien,
Südliche Frankenalb). — Stuttg. Beitr. Naturk., Ser. B., 16, 143 pp., 11 pls., 18 figs., 3 tabs.;
Stuttgart.

OERTLI, H. J. (1965): Ostrakoden der Neuburger Bankkalke (Mittl. Tithon) von Neuburg an der ı
Donau, Südbayern. — Mitt. Bayer. Staatssamml. Paläont. hist. Geol., 5, p. 127-135, pl.
11—12; München.

QUENSTEDT, F. A. (1843): Das Flözgebirge Würtembergs. Mit besonderer Rücksicht auf den Jura.
560 pp.; Tübingen (Fues).
— (1858): Der Jura. VI + 842 pp., 100 + 3 pls., 42 figs.; Tübingen (Laupp).
REıFrr, W. (1958): Beiträge zur Geologie des Albuchs und der Heidenheimer Alb (Württemberg). —
Arb. geol.-paläont. Inst. T. H. Stuttgart, n. F. 17, 142 pp., 10 figs., 1 suppl.; Stuttgart.

ZIEGLER, THE WHITE JURASSIC IN S GERMANY 53

Rot, A. (1931): Die Stratigraphie des Oberen Malm im Lauchertgebiet (Schw. Alb) als Grund-
lage für tektonische Untersuchungen. — Abh. Preuss. geol. Landesanst., n. F. 135, 164 pp,
7 pls., 22 figs.; Berlin.

SAPUNOV, I. G. & ZIEGLER, B. (1976): Stratigraphische Probleme im Oberjura des westlichen Bal-
kangebirges. — Stuttg. Beitr. Naturk., B, 18, 47 pp., 3 pls., 14 figs.; Stuttgart.

SCHÄDEL, K. (1962): Die fossilen Schwammriffe der Schwäbischen Alb. — Die Natur, 70, p. 53—60,
6 figs., p. 97—102, 4 figs.; Schwäbisch Hall.

ScHALL, W. (1964): Die Geologie der Blätter Deggingen, Geislingen a. d. Steige und Weidenstetten
(Nr. 7424, 7325 und 7425) 1:25 000 (Schwäbische Alb). — Arb. geol.-paläont. Inst. T. H.
Stuttgart, n. F. 46, 260 pp., 10 pls., 2 figs., 3 tabs.; Stuttgart.

SCHMIDT-KALER, H. (1962): Zur Ammonitenfauna und Stratigraphie des Malm «a und £ in der
Südlichen und Mittleren Frankenalb. — Erlanger geol. Abh., 43, 12 pp., 2 pls., 2 figs.;
Erlangen. — [1962a]

— (1962): Stratigraphische und tektonische Untersuchungen im Malm des nordöstlichen Ries-
Rahmens. Nebst Parallelisierung des Malm Alpha bis Delta der Südlichen Frankenalb über
das Riesgebiet mit der schwäbischen Ostalb. — Erlanger geol. Abh., 44, 51 pp., 5 pls., 16
figs.; Erlangen. — [1962b]

SCHMIERER. TH. (1902): Das Altersverhältnis der Stufen „Epsilon“ und „Zeta“ des weissen Jura. —
Z. Deutsch. geol. Ges., 54, p. 525—607, 14 figs.; Berlin.

SCHNEID, TH. (1915): Die Ammonitenfauna der obertithonischen Kalke von Neuburg a. D. —
Geol. paläont. Abh., n. F. 13/5, p. 305—416, pl. 17—29, 1 fig.; Jena. f
SCHNEIDER, J. (1957): Stratigraphie und Entstehung der Zementmergel des Weißen Jura in
Schwaben. — Arb. geol.-paläont. Inst. T. H. Stuttgart, n. F. 11, 94 pp., 4 pls., 10 figs.;

Stuttgart.

SCHRAMMEN, A. (1936): Die Kieselspongien des oberen Jura von Süddeutschland. — Palaeonto-
graphica, A, 84, p. 149—194, pl. 14—23; 85, p. 1—114, pl. 1—17; Stuttgart. -

SCHREINER, A. (1961): Über den Weißen Jura im Hegau. — Jh. geol. Landesamt Baden-Württem-
berg, 5, p. 243—277, pl. 25—26, fig. 20—22, tab. 15—17; Freiburg im Breisgau.

SEEGER, D. (1961): Die Delta=Epsilon=Grenzschichten im schwäbischen Weißen Jura. — Jber. Mitt.
oberrhein. geol. Ver., n. F. 43, p. 49—72, pl. 3, 9 figs.; Stuttgart.

SEIBOLD, E. (1950): Der Bau des Deckgebirges im oberen Rems-Kocher-Jagst-Gebiet. — N. Jb.
Geol. Paläont., Abh., 92, p. 243—366, pl. 3, 17 figs., 12 tabs.; Stuttgart.

— (1952): Chemische Untersuchungen zur Bankung im unteren Malm Schwabens. — N. Jb. Geol.
Paläont., Abh., 95, p. 337—370, 11 figs., 2 tabs.; Stuttgart.

SEIBOID, E. & I. (1953): Foraminiferenfauna und Kalkgehalt eines Profils im gebankten unteren
Malm Schwabens. — N. Jb. Geol. Paläont., Abh., 98, p. 28—86, pl. 4-6, 5 figs.; Stuttgart.

— (1960): Foraminiferen der Bank- und Schwamm-Fazies im unteren Malm Süddeutschlands. —
N. Jb. Geol. Paläont., Abh., 109, p. 309-438, pl. 7—8, 22 figs., several tabs.; Stuttgart.

SEILACHER, A. (1963): Umlagerung und Rolltransport von Cephalopoden-Gehäusen. — N. Jb. Geol.
Paläont., Mh., 1963/11, p. 593—615, 9 figs.; Stuttgart.

Sör, H. (1954): Dogger-Profile aus dem Teufelsloch bei Bad Boll (Württemberg, mittlere Schwä-
bische Alb). — Jber. Mitt. oberrhein. geol. Ver., n. F. 35 (1953), p. 43—53; Stuttgart.
STAHLECKER, G. (1934): Stratigraphie und Tektonik des Braunen Jura im Gebiet des Stuifen und
Rechberg. — Jh. Ver. vaterl. Naturkde. Württ., 90, p. 59—121, 2 pls., 1 fig.; Stuttgart.
STREIM, W. (1960): Geologie der Umgegend von Beilngries (Südliche Frankenalb). — Erlanger geol.

Abh., 36, 15 pp., 6 figs., 1 map; Erlangen.

— (1961): Stratigraphie, Fazies und Lagerungsverhältnisse des Malm bei Dietfurt und Hemau
(Südliche Frankenalb). — Erlanger geol Abh., 38, 49 pp., 25 figs., 1 map; Erlangen.

TEMMLER, H. (1964): Über die Schiefer- und Plattenkalke des Weißen Jura der Schwäbischen Alb
(Württemberg). — Arb. geol.-paläont. Inst. T. H. Stuttgart, n. F. 43, 106 pp., 24 pls., 18
figs., 2 tabs.; Stuttgart.

TERZIDIS, A. (1966): Der Braune Jura im Gebiet zwischen Eningen und Glems (Mittlere Schwäbi-
sche Alb, Württemberg). — Jber. Mitt. oberrhein. geol. Ver., n. F. 48, p. 31-67, 4 figs.,
1 tab.: Stuttgart.

VoGEL, K. (1959): Wachstumsunterbrechungen bei Lamellibranchiaten und Brachiopoden. Ein Bei-
trag zur Beurteilung fossiler Kleinfaunen und zur Frage „Bio- oder Thanatocoenose“. —
N. Jb. Geol. Paläont., Abh., 109, p. 109-129, pl. 4, 9 figs., 2 tabs.; Stuttgart.

54 STUTTGARTER BEITRÄGE ZUR NATURKUNDE Ser. B, Nr. 26

WAGENPLAST, P. (1972): Ökologische Untersuchung der Fauna aus Bank- und Schwammfazies
des Weißen Jura der Schwäbischen Alb. — Arb. Inst. Geol. Paläont. Univ. Stuttgart, n. F.
67, p. 1—99, pl. 1—18, 10 figs., 5 tabs.; Stuttgart.

WAGNER, G. (1960): Einführung in die Erd- und Landschaftsgeschichte mit besonderer Berücksich-
tigung Süddeutschlands. 3rd ed., 694 pp., 234208 pls., 591 figs.; Öhringen (Rau).

WAGNER, W. (1965): Spongien aus den Neuburger Bankkalken (Mittel-Tithon) von Neuburg an
der Donau. — Mitt. Bayer. Staatssamml. Paläont. hist. Geol., 5, p. 23—27, pl. 2; München.

WEILER, H. (1957): Untersuchungen zur Frage der Kalk-Mergel-Sedimentation im Jura Schwabens. —
Thesis Univ. Tübingen, 58 pp., 45 figs. — [Mscr.]

WELLNHOFER, P. (1964): Zur Pelecypodenfauna der Neuburger Bankkalke (Mittel-Tithon). — Abh.
Bayer. Akad. Wiss., math.-naturwiss. Kl., n. F. 119, 143 pp., 7 pls., 69 figs., 2 tabs.;
München.

WINTER, B. (1970): Foraminiferenfaunen des Unter-Kimmeridge (mittlerer Malm) in Franken. —
Erlanger geol. Abh., 79, 60 pp., 4 pls., 35 figs., Erlangen.

WIRTH, E. (1958): Die Schichtenfolge der Erdölaufschlußbohrung Buttenhausen 1, Schwäbische Alb.
— Jber. Mitt. oberrhein. geol. Ver., n. F. 40, p. 107—128, 3 figs.; Stuttgart.
— (1960): Die Schichtenfolge der Erdölaufschlußbohrung Upflamör 1, Schwäbische Alb. — Jber.
Mitt. oberrhein. geol. Ver., n. F. 42, p. 129—160, 4 figs.; Stuttgart.

WUNDT, G. (1883): Über die Vertretung der Zone des Ammonites transversarius im schwäbischen
weissen Jura. — Jh. Ver. vaterl. Naturkde. Württ., 39, p. 148—165, 2 figs., 1 tab.; Stuttgart.

YAMAaNI, S.-A. (1973): Zur Bivalvenfauna der Korallenkalke von Laisacker bei Neuburg a. d.
Donau (Unter-Tithon). — Thesis Univ. München. 216 + XVI pp., 6 pls., 47 figs., 7 tabs.;
München.

— (1975): Bivalven-Fauna der Korallenkalke von Laisacker bei Neuburg a d. Donau. Unteres
Tithonium, Bayern. — Palaeontographica, A, 149, p. 31—118, pl. 14—19, 43 figs., 5 tabs.;
Stuttgart.

— (1976): Revision der Bivalvenfauna der Kelheimer Diceraskalke (Untertithon, Bayern). —
Mitt. Bayer. Staatssamml. Paläont. hist. Geol., 16, p. 5—10; München.

YAMANI, S.-A. & SCHAIRER, G. (1975): Bivalvia aus dem Dolomit von Großmehring bei Ingol-
stadt (Untertithon, Südliche Frankenalb, Bayern). — Mitt. Bayer. Staatssamml. Paläont.
hist. Geol., 15, p. 19—27, pl. 3, 4 figs.; München.

ZAKRZEWSKI, A. J. A. (1887): Die Grenzschichten des Braunen zum Weissen Jura in Schwaben. —
Jh. Ver. vaterl. Naturkde. Württ., 43, p. 87—141, pl. 1—2; Stuttgart.

Zeıss, A. (1955): Stratigraphie des Callovien und Unter-Oxfordien bei Blumberg (Südbaden). —
Jh. geol. Landesamt Baden-Württemberg, 1, p. 239-266, pl. 9—10, fig. 29—31; Freiburg ı
im Breisgau.

— (1957): Die ersten Cardioceraten-Faunen aus dem oberen Unter-Oxfordien Süddeutschlands
und einige Bemerkungen zur Dogger/Malm-Grenze. -- Geol. Jb., 73, p. 183—204, 2 tabs.; ;
Hannover.

— (1966): Biostratigraphische Auswertung von Ammonitenaufsammlungen im Profil des Malm ı
o und £ am Feuerstein bei Ebermannstadt/Ofr. — Erlanger geol. Abh., 62, p. 104—111,
tab. 6; Erlangen,

— (1968): Über Stratigraphie und Faziesräume des Malm der Frankenalb — Jber. Mitt. ober-
rhein. geol. Ver., n. F. 50, p. 101—114, 2 figs.; Stuttgart. — [1968a]

— (1968): Untersuchungen zur Paläontologie der Cephalopoden des Unter-Tithon der Südlichen
Frankenalb. — Abh. Bayer. Akad. Wiss., math.-naturwiss. Kl., n. F. 132, 190 pp., 27 pls.,
17 figs.; 6 tabs.; München. — [196sb]

— (1977): Jurassic stratigraphy of Franconia. — Stuttg. Beitr. Naturk., Ser. B, 31, 32 pp., 8 figs.;
Stuttgart.

ZIEGLER, B. (1955): Die Sedimentation im Malm Delta der Schwäbischen Alb. — Jber. Mitt. ober-
rhein. geol. Ver., n. F. 37, p. 29-55, 7 figs.; Stuttgart.
— (1958): Feinstratigraphische Untersuchungen im Oberjura Südwestdeutschlands — ihre Be-
deutung für Paläontologie und Paläogeographie. — Eclogae geol. Helvet., 51, p. 265—278,
6 figs.; Basel. — [1958a]
— (1958): Die Ammonitenfauna des tieferen Malm Delta in Württemberg. — Jber. Mitt.
oberrhein. geol. Ver., n. F. 40, p. 171—201, 4 figs.; Stuttgart. — [1958b]

ZIEGLER, THE WHITE JURASSIC IN S GERMANY 55

(1959): Profile aus dem Weißjura ö der Schwäbischen Alb. — Arb. geol.-paläont. Inst. T. H.
Stuttgart, n. F. 21, 70 pp., 5 fig.; Stuttgart.

(1962): Die Ammoniten-Gattung Aulacostephanus im Oberjura (Taxionomie, Stratigraphie,
Biologie). — Palaeontographica, A, 119, p. 1—172, pl. 1—22, 85 figs., 5 tabs.; Stuttgart.
(1964): Das untere Kimeridgien in Europa. — Coll Jurass. Luxembourg 1962, C. r. Mem.
Inst. grand-ducal, Sect. Sci. natur., phys., math., p. 345—354; Luxembourg.

(1967): Ammoniten-Ökologie am Beispiel des Oberjura. — Geol. Rundschau, 56, p. 439—

467, 20 figs.; Stuttgart.

56

Fig.

Fig.

Fig.

Fig.

Fig.

Fig.

Fig.

STUTTGARTER BEITRÄGE ZUR NATURKUNDE

Plate ı

Perisphinctes (Arisphinctes) elisabethae (DE Rıaz).
Lower White Jurassice @ (transversarinm zone), Blumberg. — Natural size.

Ochetoceras hispidun (OPPEL).

Ser. B, Nr. 26

Lower White Jurassic @ (transversariunm zone), Laufen an der Eyach. — Natural size.

Gregoryceras romani (DE GROSSOUVRE).

Lower White Jurassic « (transversarium zone), Blumberg. — Natural size.

Dichotomoceras bifurcatus (QUENSTEDT).
Lower White Jurassic @«, Blumberg. — Natural size.

Trimarginites arolicus (OPPEL).

Lower White Jurassic @ (transversarium zone), Blumberg. — Natural size.

Epipeltoceras bimamnmıatum (QUENSTEDT).
Upper White Jurassic « (bimammatum zone), Lochen. — Natural size.

Amoeboceras alternans (von Buch).
Upper White Jurassic @ (bimammatum zone), Lochen. — Natural size.

Fig. 1--7: Staatliches Museum für Naturkunde in Stuttgart.

ZIEGLER, THE WHITE JURASSIC IN S GERMANY

57

58 STUTTGARTER BEITRÄGE ZUR NATURKUNDE Ser. B, Nr. 26

Plate 2

Fig. 1. Taramelliceras costatum (QUENSTEDT).
White Jurassic # (planula zone), Laufen an der Eyach. — Natural size.

Fig. 2. laoceras (Subnebrodites) laxevolutum (FONTANNES).

White Jurassic # (planula zone), Unterweckerstell near Donzdorf. — Natural size.
Fig. 3. Sutneria galar (OPPEL).

Upper White Jurassic # (planula zone, galar subzone), Immendingen. — Natural size.
Fig. 4. Amoeboceras lineatum (QUENSTEDT).

White Jurassic # (planula zone), Nendingen. — Natural size.
Fig. 5. Orthosphinctes tiziani (OPPEL).

White Jurassic # (planula zone), Laufen an der Eyach. — Natural size.
Fig. 6. Glochiceras (Lingulaticeras) lingulatum (QUENSTEDT).

White Jurassic # (planula zone), Braunenberg near Aalen. — Enlarged x 1,5.
Fig. 7. Taramelliceras falculunı (QUENSTEDT).

White Jurassic # (planula zone), Fürsitz near Aalen. — Enlarged x 1,5.

Fig. 1—6: Staatliches Museum für Naturkunde in Stuttgart.

Fig. 7: Institut und Museum für Geologie und Paläontologie der Universität Tübingen.

ZIEGLER, THE WHITE JURASSIC IN S GERMANY 59

60 STUTTGARTER BEITRÄGE ZUR NATURKUNDE Ser. B, Nr. 26

Plate 3

Fig. 1. Ataxioceras (Parataxioceras) planulatum (QUENSTEDT).
White Jurassic y (hypselocyclum zone), Albstadt-Truchtelfingen. — Natural size.

Fig. 2. Ataxioceras (Ataxioceras) hypselocyclum (FONTANNES).
White Jurassic y (hypselocyclum zone), Unterkochen. — Natural size.

Fig. 3. Sutneria platynota (REINECKE).
Lower White Jurassic y (platynota zone), Swabian Alb. — Natural size.

Fig. 4. Creniceras dentatum (REINECKE).
White Jurassic y (hypselocyclum zone), Weckerstell near Donzdorf. — Enlarged x 1,5.

Fig. 5. Idoceras (ldoceras) balderum (OPPpe1).
Upper White Jurassic y (divisum zone), Swabian Alb. — Natural size.

Fig. 6. Streblites tenuilobatus (OPper).
White Jurassic y (probably hypselocyclum zone), Laufen an der Eyach. — Natural size.

Fig. 1—3, 5, 6: Staatliches Museum für Naturkunde in Stuttgart.

Fig. 4: Institut und Museum für Geologie und Paläontologie der Universiät Tübingen.

61

ZIEGLER, THE WHITE JURASSIC IN S GERMANY

62 STUTTGARTER BEITRÄGE ZUR NATURKUNDE

Plate 4

Fig. 1. Aspidoceras acanthicum (OPPEL).
Lower White Jurassic ö (acanthicum zone), Swabian Alb. — Reduced x ?/s.

Fig. 2. Katroliceras (Crussoliceras) divisum (QUENSTEDT).
Upper White Jurassic y (divisum zone), Bartholomä. — Reduced x !».

Fig. 1—2: Staatliches Museum für Naturkunde in Stuttgart.

Ser. B, Nr. 26

63

ZIEGLER, THE WHITE JURASSIC IN S GERMANY

64

Fig.
Fig.
Fig.
Fig.
Fig.

Fig.

STUTTGARTER BEITRÄGE ZUR NATURKUNDE Ser. B, Nr. 26
Plate 5

1. Aulacostephanus (Aulacostephanus) pseudomutabilis (DE LORIOL).

Upper White Jurassic ö (eudoxus zone), Bräunesberg near Nendingen. — Natural size.
2. Aulacostephanus (Aulacostephanoceras) eudoxus (D’ORBIGNY).

Upper White Jurassic ö (eudoxus zone), Blaubeuren. — Natural size.
3. Aulacostephanus (Aulacostephanites) eulepidus (SCHNEID).

Lower White Jurassic ö (acanthicum zone), Tuttlingen. — Natural size.
4: Sutneria eumela (D’ORBIGNY).

Upper White Jurassic ö (eudoxus zone), Stetten an der Donau. — Natural size.
5. Orthaspidoceras schilleri (OPPpE1).

White Jurassic ö (lower eudoxus zone), Hülben near Urach. — Reduced x ?/s.

1—5: Staatliches Museum für Naturkunde in Stuttgart.

ZIEGLER, THE WHITE JURASSIC IN S GERMANY 65

66

Fig.

Fig.

Fig.

Fig.

Fig.

AWP}

STUTTGARTER BEITRÄGE ZUR NATURKUNDE Ser. B, Nr. 26

Plate &
Hybonoticeras beckeri (NEUMAYR).
White Jurassic & (probably subeumela subzone), Herrlingen. — Natural size.
Sutneria subeumela (SCHNEID).
White Jurassic & (beckeri zone, subeumela subzone), Herrlingen. — Natural size.

Oxyoppelia fischeri (BERCKHEMER).
White Jurassic & (beckeri zone, probably subeumela subzone), Herrlingen. — Natural size.

Virgataxioceras setatum (SCHNEID).
Upper White Jurassic & (beckeri zone, setatum subzone), Kolbingen. — Natural size.

Gravesia gigas (ZIETEN).
Upper White Jurassic © (“Hangende Bankkalke“), Riedlingen, — Natural size.

Fig. 1--5: Staatliches Museum für Naturkunde in Stuttgart.

ZIEGLER, THE WHITE JURASSIC IN S

GERMANY

67

68 STUTTGARTER BEITRÄGE ZUR NATURKUNDE Ser. B, Nr. 26

Plate 7

Fig. 1. Hybonoticeras hybonotum (OPPEL).
Upper White Jurassic © (“Hangende Bankkalke“), Riedlingen. — Reduced x !/z

Fig. 2. Lithacoceras ulmense (OPPpE1).
Lower White Jurassic © (“Liegende Bankkalke“), Ulm region. — Natural size.

Fig. 1: Staatliches Museum für Naturkunde in Stuttgart.
Fig. 2: Bayerische Staatssammlung für Paläontologie und Historische Geologie München

ZIEGLER, THE WHITE JURASSIC IN S GERMANY 69

70

STUTTGARTER BEITRÄGE ZUR NATURKUNDE Ser. B, Nr. 26

Plaue 19

Ammonites of the middle and upper part of the Lower Tithonian of the Franconian Alb

Fig. 1: Usseliceras parvinodosum ZEISS

Fig.

Fig.

Fig.

Fig.

Fig.

Large specimen: holotype; smal! specimen: paratype.

Lower Rennertshofen formation, Bertoldsheim member.

Ammerfeld W.

Bayerische Staatssammlung für Paläontologie u. Historische Geologie München, no. 1948 1/22.
Reduced x ta.

: Usseliceras tagmersheimense ZEIss, holotype.
Usseltal formation, Tagmersheim member.
Tagmersheim.
Geologisches Institut der Universität Erlangen, no. 5 30.
Reduced x !/a.

: Danubisphinctes palatinus Zeıss, holotype.
Upper Rennertshofen formation, Finkenstein member.
Ellenbrunn.
Geologisches Institut der Universität Erlangen, no. S 250.
Reduced x !/a.

: Dorsoplanitoides triplicatus Zeiss, holotype.
Lower Rennertshofen formation, Bertoldsheim member.
Bertoldsheim.
Geologisches Institut der Universität Erlangen, no. 5 132.
Reduced x Ya.

: Franconites vimineus (SCHNEID), paratype.
Middle Rennertshofen formation, Ammerfeld member.
Rohrbach S.
Geologisches Institut der Universität Erlangen, no. 5 510.
Reduced x !/».

: Neochetoceras mucronatum BERCKHEMER & HÖLDER.
Usseltal formation, Tagmersheim member.
Hagenau.
Geologisches Institut der Universität Erlangen, no. 5 728.

Reduced x !/a.

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72 STUTTGARTER BEITRÄGE ZUR NATURKUNDE Ser. B, Nr. 26

Blattes
Fossils of the sponge-algal facies

Fig. 1. Stauroderma lochense (QUENSTEDT).
Skeleton of the hexactinellid sponge worked out by acid. Upper Oxfordian (bimammatum
zone), Streitberg (Franconia). — Reduced x a.

Fig. 2, 3. Lacunosella trilobata (ZIETEN).
Kimmeridgian, Swabian Alb. — Reduced x ?/a.

Fig. 4. Cnemidiastrum stellatum (GOLDFUSS).
Calcified sponge “nummy“. Lower Kimmeridgian, Lochen region. — Reduced x ?/a.

Fig. 5. Lower surface of a hexactinellid sponge settled by serpulids and the bryozoan Berenicea.

Upper Oxfordian (upper White Jurassic a, bimammatum zone), Bärenthal. — Enlarged x 3,5.
Fig. 1—4: Staatliches Museum für Naturkunde in Stuttgart.
Fig. 5: Paläontologisches Institut und Museum der Universität Zürich.

73

ZIEGLER, THE WHITE JURASSIC IN S GERMANY

74

Fig.

Fig.

Fig.

Fig.

Fig.

Fig.

Fig.

Fig.

Fig.
Fig.
Fig.
Fig.
Fig.
Fig.

Fig.

STUTTGARTER BEITRÄGE ZUR NATURKUNDE Ser. B, Nr. 26

Plate 9
Fossils of the Lochen facies

Amoeboceras alternans (v. BucH), phragmocone.
Upper Oxfordian (bimammatum zone), Lochen near Balingen. — Enlarged x 2.

Epipeltoceras semiarmatum (QUENSTEDT).
Upper Oxfordian (bimammatum zone), Lochen near Balingen. — Enlarged x 2.

3,4. Taramelliceras pichleri (OPPper).

5%

Upper Oxfordian (bimammatum zone), Lochen near Balingen. — Enlarged x 2.

Taramelliceras lochense (OPPEL).
Upper Oxfordian (bimammatum zone), Lochen near Balingen. — Enlarged x 2.

6,7. Glochiceras canale (QUENSTEDT).

Upper Oxfordian (bimammatum zone), Lochen near Balingen. — Enlarged x 2.

8—10. Trigonellina pectunculus (SCHLOTHEIM).

Upper Oxfordian (bimammatum zone), Lochen near Balingen. — Enlarged x 2.

11—12. Trigonellina loricata (SCHLOTHEIM).

13.

Upper Oxfordian (bimammatum zone), Mühlheim an der Donau. — Enlarged x 2.

Nucleata aucleata (SCHLOTHEIM).
Probably lower Kimmeridgian (platynota or hypselocyclum zones), Lochen region near
Balingen. — Enlarged x 2.

14—15. Tylasteria jurensis (QUENSTEDT), marginal plates of sea stars.

16.

117%

18.

19.

20.

Upper Oxfordian (probably bimammatum zone), Geislingen. — Enlarged x 2.

Magnosia nodulosa (GOLDFUSS).
Upper Oxfordian (bimammatum zone), Lochen near Balingen. — Enlarged x 2.

Sporadopyle obligqua (GOLDFUSS), siliceous sponge.
Upper Oxfordian (bimammatum zone), Lochen near Balingen. — Enlarged x 2.

Peronidella jurassica (ETALLON), calcareous sponge, settled by a serpulid.
Upper Oxfordian (bimammatum zone), Lochen near Balingen. — Enlarged x 2.
Plegiocidaris sp.

Upper Oxfordian (bimammatum zone), Lochen near Balingen. — Enlarged x 2.

Eugeniacrinites caryophyllatus (GOLDFUSS).
Upper Oxfordian (bimammatum zone), Lochen near Balingen. — Enlarged x 2.

1—20: Staatliches Museum für Naturkunde in Stuttgart.

ZIEGLER, THE WHITE JURASSIC IN S GERMANY 75

76

Fig.

Fig.

Fig.

Fig.

Fig.

Fig.

Fig.
Fig.

Fig.
Fig.
Fig.
Jeilez,

STUTTGARTER BEITRÄGE ZUR NATURKUNDE Ser. B, Nr. 26

Plate 10
Fossils of the calcareous shales of the lower Tithonian

Saccocoma pectinata GOLDFUSS; free swimming crinoid.
Lower Tithonian (Gravesia zone, ?Solnhofen formation), “Solnhofen“, Franconia — Redu-
ced x Ya.

Glochiceras (Paralingulaticeras) lithographicum (OPPEL).
Lower Tithonian (Gravesia zone, ?Solnhofen formation), “Solnhofen“, Franconia — Redu-
ced x a.

Marks of rolling ammonites (perisphinctids).
Lower Tithonian (Gravesia zone, Solnhofen formation), Painten, Franconia. — Reduced x !».

Leptolepis, well preserved specimen, scales present.

Lower Tithonian (Gravesia zone, Solnhofen formation), “Eichstätt“, Franconia. Reduced
x Ua.

Leptolepis, partly disintegrated specimen.

Lower Tithonian (Gravesia zone, Solnhofen formation), Zandt, Franconia. — Reduced x /».

?Propterus, partly disintegrated specimen.
Lower Tithonian (Gravesia zone, Solnhofen or Mörnsheim formation), Mörnsheim, Fran-
conia. — Reduced x !/a.

Leptolepis, totally disintegrated specimen.
Lower Tithonian (Gravesia zone, Solnhofen formation), Zandt, Franconia. — Reduced x 1/2.

Leptolepis, partly disintegrated specimen, scales mostly missing.
Lower Tithonian (Gravesia zone, Solnhofen formation), Zandt, Franconia. — Reduced x !/a.

1: Staatliches Museum für Naturkunde in Stuttgart.

2: Bayerische Staatssammlung für Paläontologie und Historische Geologie, München.

3—4: Paläontologisches Institut und Museum der Universität Zürich.

5—8: Philosophisch-Theologische Hochschule Eichstätt.

HU

ZIEGLER, THE WHITE JURASSIC IN S. GERMANY

78

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STUTTGARTER BEITRÄGE ZUR NATURKUNDE Ser. B, Nr. 26

Plate 11
Fossils of the coral facies of the lower Tithonian

1. Arctostrea gregarea (SOWERBY).
Lower Tithonian (Gravesia zone), Nattheim. — Enlarged x 3.

2. Juralina insignis (ZIETEN).
Lower Tithonian (Gravesia zone), Nattheim. — Natural size.

3. Cheirothyris trigonella (SCHLOTHEIM).
Lower Tithonian (Gravesia zone), Nattheim. — Enlarged x 2,5.

4. Thecosmilia trichotoma (GOLDFEUSS).
Lower Tithonian (Gravesia zone), Nattheim. The coral is settled by serpulids, an oyster, and

a calcareous sponge. — Natural size.

5. A gastropod of the family Nerineidae embedded in a bioclastic limestone.
Lower Tithonian (Gravesia zone), Nattheim. — Enlarged x 1,25.

6. Plegiocidaris coronata (GOLDFUSS).
Lower Tithonian (Gravesia zone), Nattheim. — Enlarged x 1,25.

1—6: Staatliches Museum für Naturkunde in Stuttgart.

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