SEDIMENTARY
GEOLOGY
ELSEVIER
Sedimentary Geology 102 (1996) 111-130
Response of shallow-marine carbonate facies to third-order
and high-frequency sea-level fluctuations: Hauptrogenstein
Formation, northern Switzerland
Ramon Gonzalez 1
Rosenstiel School of Marine and Atmospheric Science, Division of Marine Geology and Geophysics, 4600 Rickenbacker Causeway,
Miami, FL 33149, USA
Received 28 August 1993; revised version accepted 29 January 1994
Abstract
Facies patterns in shallow-marine carbonates of the Hauptrogenstein Formation of northern Switzerland (middle
Bajocian to early Bathonian) reflect small changes in sea level. Third-order sea-level fluctuations, calculated from
large-scale facies patterns (alternations of marl- and carbonate-dominated sedimentary units on the level of
members) and subsidence, show two phases of sea-level rise and fall in the late Bajocian and a relative sea-level rise
in the early Bathonian. Most of the sedimentary rocks were produced during phases of relative rise and highstand of
sea level. No periods of emergence during lowstands are preserved.
Sea-level changes of a higher order have been analyzed by facies changes at the outcrop scale. Thin shallowing-up
parasequences (0.5-6 m thick) have been correlated across platform, ramp and offshore sedimentary environments.
In each of these environments carbonates react differently to sea-level fluctuations. Relative rises in sea level are
represented by non-deposition and biogenic sediments, periods of stable or slightly falling sea level are dominated by
oolitic sediments: (1) in the offshoal environment, marl layers at the base of thin shallowing-up units are covered by
increasingly proximal tempestites; (2) in the ramp environment, oblique-stratified, oolitic and bioclastic grainstones
are bounded by marine flooding surfaces; (3) on the platform, marine flooding surfaces are overlain by beds
deposited under moderate-energy conditions (coral beds, oncoid beds, platform tempestites) which are in turn
covered by high-energy, oblique-stratified oolitic grainstones.
Such parasequences, deposited in response to small-scale, high-frequent3, sea-level changes can be correlated
over distances of more than 100 km. A model for evolution and response of carbonate facies to sea-level changes is
presented.
I. Introduction
In this paper, I present a regional study of the
Bajocian to early Bathonian Hauptrogenstein
t Present address: Dept. of Engineering Science, Oxford
University, Parks Road, Oxford OX1 3PJ, UK.
Elsevier Science B.V.
SSDI 0037-0738(95)00059-3
Formation of northern Switzerland where I show
how carbonates in a tidal, oolitic environment
react to sea-level changes and subsidence and
how facies changes can be used as a tool to
determine sea-level fluctuations on a range of
scales.
Studies of the effects of high-frequency relative sea-level changes in carbonates show that
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R. Gonzalez/Sedirnentary Geology 102 (1996) 111-130
113
Platform geometry of the Hauptrogenstein Formation (very schematic)
shallowing-up
successions
3r d
~_ _
biochronozones
and subzones
W
_ ~;. . . .
2 nd
)nes
~s
1st
Fbzone
high
IowJ
subsidence (qualitative)
/
(sub-)zone limits
idealized parasequence
boundaries
lower and eastern lithostratigraphic limits of the
Hauptrogenstein Formation
platform and ramp
facies-belts(shallow water
carbonates dominate)
offshoal facies-belts
(marls and clays dominate)
ca. 20
-]
mI
ca. 20km
Fig. 2. Simplified W - E cross-section through the Hauptrogenstein Formation including the lithostratigraphic units mentioned in
this paper. The Rothenfluh Beds are not part of the Hauptrogenstein Formation in a lithostratigraphic sense, but are included in
the first shallowing-up succession. The Klingnau Formation represents offshoal sediments of the central European epicontinental
sea and is coeval with the Hauptrogenstein Formation.
facies patterns in shallow-marine carbonates are
excellent indicators of sea-level fluctuations because their formation is highly dependent on
parameters like water energy, depth and temperature (Hays et al., 1976; Goodwin and Anderson,
1985; Grotzinger, 1986; Goldhammer et al., 1990).
Patterns of facies successions have been used as
correlation tools over large distances (e.g.,
Grotzinger, 1986) and are especially useful in
regions with relatively thin deposits, like the Ba-
jocian and Bathonian of central Europe, where
geometries and thicknesses of sediment bodies
are below seismic resolution (e.g., Vail et al.,
1987; Rioult et al., 1991; Javaux, 1992).
Most carbonates--unlike siliciclastics--are
produced in situ and their production is dependent mainly on environmental parameters and not
on source area. In addition, carbonates tend to
have a different cementation behaviour than siliciclastics. For these reasons, their response to
Fig. 1. (a) Map of northern Switzerland showing location of the outcrops and wells studied within the Hauptrogenstein Formation.
(b) Idealized type section of the Hauptrogenstein Formation, including late Bajocian to earliest Bathonian biostratigraphic
ammonite zones and their relation to lithostratigraphic units and shallowing-up successions.
114
R. Gonzalez / Sedimentary Geology 102 (1996) 111-130
Table 1
Description and interpretation of carbonate facies types found within the Hauptrogenstein Formation
Facies
Imarls and
clays
characterisation of sediments and
primary sedimentary structures
typical
components
setting
genetic
mechanism
relative estimated
depth
absolute
depth(in m)
monotonous mudstones with layers of silt-sized
bioclasts, concretions or whole fossils
Pholadomya,
Homomya, different
brachiopods, sometimes
ammomtes and
belemnites
distal
offshoal
calm
water
periods
below
storm
wave-
> 25
base
bioturbated,
distal
tempestites
silt- to fine sand-sized, mostly bioclastic wacke- to packstones, sometimes with coarser bioclasts; lateral continuous
bedding, strong bioturbation
silt- to sand-sized bioclasts offshoal
(bivalves, brachiopods,
echinoderms, gastropods)
nonbioturbated
tempestites
silt- to fine sand-sized, bioclastic wacke- to packstones;
typical vertical succesions are: massive, fine to medium
sand-sized carbonatesand beds grading into layers with
ripple-like structures, sometimes hummocky-cross-stratification (sensu Harms et al., 1982), then into fine, parallel
laminated marl and silt-sized carbonatesand alternations
and then into marls
silt- to sand-sized bioclasts
(bivalves, brachiopods,
echinoderms, gastropods,
sometimes coral fragments
and oncoids)
oolitic
tempestites
partly bioturbated oolitic pack- to grainstones with planar
top and base; where the original depositional structure
is preserved, it is often a unidirectional oblique stratification
ooids, sand-to gravel-sized offshoalbioclasts (sameas above)
transition
often associatedwith
cyanophycean growths and
fungoid/bacterial borings
oblique
stratifications
dominated
by crinoids
tidal,
oolitic
grainstones
wacke- to packstones with crinoids, bioclasts and ooids;
frequent structures are unidirectional megaripples, that
show evidence for dominant southward transport
crinoid fragments
(Chariocrinus andreae
DESOR), other bioclasts,
rarely ooids
oblique stratified oolitic and bioctastic grainstones interpreted as ebb-tide dominated sand waves (type III sensu
Allen, 1980); main transport directions are towards south
platform
sand
sheets
below
storm
wavebase
> 20
near the
storm
wavebase
15-20
storms
near the
storm
wavebase
15-20
offshoaltransition
storms or
strong
tides
between
waveand storm
wave-base
10-15
ooids, sand- to gravel-sized
bioclasts (mainly
pelecypod fragments)
oolitic
shoa Is,
ramp and
platform
tides
above
wavebase
1-10
heterogenous mud- to grainstones with planar top and base,
showing only poor sorting of components and no apparent
sedimentary structures, except for an occasional fining
upward trend
ooids, micritic intraclasts
("mudclasts", "lumps"),
grapestones and a large
vanety of bioclasts (see
micritlc layers) in all
de~rees of desintesration
back-barrier storms
or
platform
below
wave-base
on the
)latform
!5-10
micritic
layers
mud- to wackestones dominated by a micritic matrix;
these beds often show strong bioturbation
gastropods, oncoids,
corals, bivalves,
brachiopods, bryozoans,
serpulid tubes, ooids
restricted,
protected
platform
calm
water
]eriods
below
wave-base
on the
~latform
5-10
coral-rich
coral associations, commonly with little vertical but a wide
lateral extension; many are not bioherms but rather biostromes, dominated by allochthonous corals; many
components show signs of abrasion and/or transport
calm
water
)eriods
and/or
storms
above
storm
wave-base
5-15
above
storm
wave-base
5-15
beds
(Thalassinoides, Chondrites)
proximal
storms
offshoal
to offshoal- l
transition
: corals (mainly Isastrea,
platform
Thamnastrea, sometimes
or
Montlivaltia), echinoids,
barrier
8/_aystropods,serpulid tubes,
chltes
storms
oncolitic
beds
oncolitic wacke- to packstones often found in association
with a micritic mamx ("oncomicrites"). This is probably
only the last station of longer transport paths from higher
to lower energyareas (as some of the oold-cores of oncoids
show); oncoidbeds can have a fining-up trend if not
bioturbated
oncoids, corals and
pelecypod fragments
channel
deposits
most channel deposits are small, cutting about 0.2-1 m deep
into the underlying unit and are typically 1-3m wide; their
base often shows a lag of brachiopods, oysters and/or bivalves
and is associated with iron-rich crusts similar to hardgrounds
brachiopods (Terebratula), all environ- storms
small oysters (Ostrea
merits, but
(rip
acuminata SOWERBYI) i typical for
currents?)
oolite shoals
and ramp
platform,
storms
back-barrier
all
depths
R. Gonzalez/ Sedimentary Geology 102 (1996)111-130
sea-level fluctuations is different from that of
shallow-marine siliciclastics.
During phases of rising and high sea level
carbonate production is highest (Droxler et al.,
1983; Reijmer et al., 1988; Sarg, 1988; Eberli and
Ginsburg, 1989). The carbonate sediments react
relatively quickly to changes in ecologic a n d / o r
environmental parameters, caused by a rise in sea
level (Schlager, 1992). In the early stage of sealevel rise, carbonate production is substantially
less than the increase in new accommodation
space ('lag phase'; Read et al., 1986; Schlager,
1992). Eventually carbonate production increases
and becomes higher than the increase in new
accommodation space ('catch up' sensu Sarg,
1988; 'log phase' sensu Schlager, 1992). Finally,
sea level reaches its maximum and at this stage
carbonate production on the platform decreases
because the subtidal area, where carbonate production is highest, is reduced due to a lack of
newly created accommodation space ('keep up'
sensu Sarg, 1988). During phases of low sea level
the biggest contributors to sedimentation are of
terrigenous character or reworked carbonate
clasts (e.g., Schlager, 1992).
2. Geological setting: litho- and biostratigraphic
framework
The Hauptrogenstein Formation of northern
Switzerland is middle Bajocian to early Bathonian in age (Fig. 1; Miihlberg, 1900; Schmassmann, 1945; Gonzalez, 1993). It is an excellent
example of an oolitic carbonate platform, which
were abundant in the shallow, epicontinental seas
along the borders of the mid-Jurassic Tethys
ocean (Hallam, 1975), surrounded by small land
areas, such as the Bohemian Massif or the remnants of the Alemannic Land.
The Hauptrogenstein Formation can be divided into three major shallowing-up successions.
A simplified sketch of the platform geometry in
an E - W direction, including lithostratigraphic
units and their age is shown in Fig. 2. Typical
facies types are characterised in Table 1.
115
2.1. Large-scale shallowing-up successions
The sedimentary succession from the Rothenfluh Beds to the top of the Lower Oolitic Series is
interpreted as a shallowing-up succession.
The Rothenfluh Beds (included in the first
shallowing-up succession even though they do not
belong to the Hauptrogenstein Formation in
terms of lithostratigraphy, cf. Fig. 2) were deposited during the blagdeni subzone. They are
dominated by din-thick marl and clay layers alternating with dm-thick bioclastic wacke- to packstones. The fine-grained bioclastic horizons become more frequent and thicker towards the top
of the Rothenfluh Beds. In the western part of
the studied area, primary sedimentary structures
are preserved, showing oblique and hummocky
cross stratifications (sensu Harms et al., 1982),
whereas in the east these layers are thinner and
bioturbated.
The base of the Hauptrogenstein Formation
(Lower Acuminata Beds) is diachronous, near the
top of the blagdeni subzone in the west of the
study area and within the niortense/subfurcatum
zone in the east (Fig. 2). The Lower Acuminata
Beds are characterised by sediments similar to
those of the Rothenfluh Beds, with the difference
that marl layers are only cm-thick and the bioclastic sediments contain dark coated ooids (the
colour is caused by organic impregnation a n d / o r
cyanophycean growths) and crinoid fragments.
The Lower Acuminata Beds are overlain by wellsorted, oolitic (average diameter 0.25-0.5 mm)
and bioclastic oblique stratified grainstones
(Lower Oolitic Series). This broad, oolitic belt
covered the eastern half of the study area at the
beginning of the garantiana zone. At the same
time, the western areas of the platform were
dominated by micritic sediments, commonly in
association with patchy coral accumulations, oncoids and ooids.
During the garantiana zone, progradation rates
of the oolitic belt towards the east decreased. In
the west coarse-grained bioclastic deposits alternate with lenses of micritic sediment and oblique
stratified, oolitic grainstones. Coral-rich layers,
containing allochthonous as well as autochthonous corals are common. Local, subma-
R. Gonzalez / Sedimentary Geology 102 (1996) 111-130
116
ca. I Okm
platform
barrier and
back-barrier
barrier and
ramp
J
offshoal
mean sea-level
l
Legend:
marl, clay
oolitic and
bioclastic grainstones
micritic mudto wackestones
~
Hi:.~::;'E:.!'::i~
ii:: .j::::i
....~.~:i~il~:~......................
L
~
head corals, patch reefs
bioturbation
~
coral detritus
channel deposits
~
oncoids
local, submarine
hardgrounds
oblique stratification
~
ca.
5m
Fig. 3. Examples of small-scale, shallowing-up units and their respective sedimentary environment. There is a trend of deposition
under increasing energy towards the top of the small shallowing-up units in all environments. All kinds of transitional forms are
present between the illustrated types, mainly dependent on local paleogeographic environmental parameters. This is especially true
for the platform realm, where a large variety of facies types is found.
rine hardgrounds often cover small-scale sedimentary units. The top of the Lower Oolitic
Series is bounded by a synchronous hardground,
which is found in all sections. Horizons classified
as hardgrounds within the Hauptrogenstein Formation show iron crusts and eroded Trypanites
and Gastrochaenolites borings. These horizons
were commonly colonized with oysters and occasionally corals. All the hardgrounds found within
the Hauptrogenstein Formation are submarine
(Trabold, 1990; Allia, 1991).
The sediments of the Rothenfluh Beds have
been interpreted as deposits of a distal 'offshoal'
setting below storm-wave base with an apparent
shallowing-upward facies trend. The bioclastic
layers were probably deposited by storms. The
same is true for the Lower Acuminata Beds, but
deposition probably took place in a much more
Fig. 4. (a) View of the quarry wall of Auenstein (for location see Fig. 1). Assumed limits of small-scale, shallowing-up units
(parasequences) are marked by arrows. The sketch shows the mid-section of the Lower Oolitic Series, about 20 m above the Lower
Acuminata Beds. The slight angle between some erosional surfaces is typical for progradational geometries in the ramp setting (the
sand waves prograde towards south). (b) Model of a small-scale shallowing-up unit (parasequence) in the barrier and ramp setting,
with all its typical attributes. Wavy, internal erosional surfaces reflect autocyclic progradation of the sand bodies, periodically
interrupted by phases of erosion and non deposition. All features within sand wave sets are typical for sand waves generated by a
ebb-tide-dominated tidal regime (sand waves of type III; Allen, 1980). The only evidence for sediment movement during floods are
convex upward reactivation surfaces (cf. McCabe and Jones, 1977; De Mowbray and Visser, 1984; Houthhuys and Gullentops,
1988). These appear only periodically and were formed when flood currents were strong enough to erode sediments from the front
of the sand waves. (c) Schematic drawing of a sand wave foreset, probably corresponding to the sediments deposited during one
ebb tide. The components are usually excellently sorted and show a continuous fining-up trend. Coarse bioclasts accumulate in the
lower portions of the foresets due to avalanching (Allen, 1984). Mud drapes at the base of the foresets and small ripples climbing
upward are probably caused by flow separation and the formation of large eddies at the front of the sand wave, rather than flood
currents.
4a
ca2m ]
•
j
~
1
~
~
4b
channel
~-'convex upward
2-5m
~
.
~
~
foreset
shallowing- I
sand
{
wave set
convex upward
reactivation surface
single, migrating dune
4c
0.2-
2m
~
~
-
•-
~
-
~
'
~
~
~
/
"
ipp
II~,mbing
les( oolitic)
-l--~J
wavy, internal
erosional surface
\ limited
'
( by .
eros ona
horizons
118
R. Gonzalez / Sedimentary Geology 102 (1996) 111-130
proximal setting ('offshoal transition'), as suggested by allochthonous ooids.
The oblique stratified, oolitic grainstones of
the Lower Oolitic Series were deposited by strong
ebb-dominated tides, producing sand waves
(Gonzalez, 1993). The setting was a 'ramp', with
deeper waters in the east and shallow oolite
shoals in the central part of the study area. West
of these oolite shoals a protected or restricted
'platform' setting became established, allowing
micritic sedimentation in quiet-water areas. Layers with coarse bioclastic components have been
interpreted as platform tempestites, similar to the
platform internal sand sheets described by Ball
(1967) in the Bahamas. Coral-rich deposits can be
considered as fossil patch reefs or coral meadows,
partly reworked by storms.
The overall sedimentation pattern of the units
above the Lower Oolitic Series is similar to the
first succession just described. Again, the succession starts with deeper-water deposits (Homomya
Marls, Upper Acuminata Beds, Fig. 2) and ends
with shallow-water ramp and platform sediments
(Upper Oolitic Series), sealed at the top by a
platform-wide, synchronous hardground. However, some differences are noteworthy. Sedimentation in the lower half of the western part of the
mapped area was dominated by offshoal sediments (Homomya Marls). The reason was probably increased, local subsidence. The central part
of the platform became a morphologic high with
an offshoal-transition-type facies (Upper Acuminata Beds). This is represented by tempestites
with reworked ooids, intraclasts and a rich, often
allochthonous fauna (echinoids, brachiopods, bivalves), deposited near storm-wave base.
A third shallowing-up succession marks the
beginning of the lowest Bathonian (zig-zag zone,
Figs. 1, 2) and starts with the marly Movelier
Beds, rich in echinoderms, brachiopods, bivalves
and coral agglomerations. They are covered by
the 'Coarse Oncolite' in the entire western part
of the platform, consisting mostly of well-rounded
oncoids (average diameter 2-4 mm) set in micritic matrix and commonly associated with gastropods (Nerinea). To the east, a wedge of echinoderm-rich carbonates ('Spatkalk') prograded
over the external platform and ramp belts into
the offshoal areas of the central European, epicontinental sea (Klingnau Formation, Fig. 2). The
Spatkalk is of the same age and younger than the
Coarse Oncolite. As with the other two successions, the third shallowing-up succession ends
with a platform-wide, synchronous hardground.
This hardground is not always well pronounced
on top of the Spatkalk. In many cases the Spatkalk
shows a fining-upward trend with successively
thicker marl layers towards its top, interpreted as
a deepening-upward succession.
2.2. Small-scale shallowing-up units
The large-scale sedimentary successions described above can be further subdivided into
small-scale, 0.5-6 m thick, shallowing-up units.
Three sedimentary environments with different
depositional styles were defined in the Hauptrogenstein Formation. In each of these environments, small-scale sedimentary units are expressed in form of vertical facies change (Fig. 3;
for facies descriptions see Table 1):
2.2.1. Offshoal and offshoal-transition facies belts
The base of the vertical successions is formed
by one or more dm-thick marl layers. They are
overlain by increasingly proximal, often bioturbated, cm- to din-thick tempestites. The same is
true for the offshoal-transition facies belt, the
only difference is the presence of thinner marl
layers and allochthonous ooids and crinoids. The
thickness of the shallowing-up units in this environment is normally in the range of 1 m.
2.2.Z Open or exposed platform facies belt ('ramp')
The dominant feature of the 'ramp' facies are
oolitic grainstones. The base of small-scale units
may be planar, but it is normally slightly wavy.
Some have post-erosional marl layers (up to 10
cm thick), with lenses of reworked ooids and
bioclasts, commonly encrusted by cyanophycean
growths.
In outcrops with good lateral exposure, the
sedimentary units show a complex internal hierarchy of erosional surfaces and sets of oblique
stratifications (Fig. 4; cf. Wetzel et al., 1993),
interpreted as tidal sand waves (sensu Allen, 1980)
R. Gonzalez / Sedtmentary Geology 102 (1996) 111-130
and reflecting the interaction between autocyclic
and allocyclic control mechanisms. The progradation of oolitic foresets was interrupted by phases
of submarine erosion, when ooid production
stopped temporarily (cf. section 4.2). Small-scale
units in the ramp environment can be up to 5-6
m thick.
2.2.3. Protected or restricted platform facies belts
Protected, 'back-barrier' areas of the platform
show a large variety of facies (Table 1). Vertical
successions typically start with a planar erosive
base, overlain by a 0.1-1 cm thick marl a n d / o r
clay horizon. These are commonly covered by
small patch reefs, coral meadows or tempestitic
layers, containing oncoids, corals, other bioclasts,
intraclasts, mudlumps and in many cases associated with a partly micritic matrix. In many tempestites one type of component dominates. The
upper part of these shallowing-up units appears
to have been deposited under the influence of
tidal currents. Here the dominant components
are ooids and bioclasts. The top of small-scale
units in the platform setting are locally marked by
a hardground. The shallowing-up units in this
environment are normally 1-2 m thick.
3. Third-order changes in relative sea level
3.1. Quantification
A curve of third-order relative sea-level change
(sensu Vail et al., 1977a, b; cf. also Allen and
Allen, 1990) for the mid-Bajocian to early Bathonian is calculated below. Only major changes in
sedimentation style on the level of members were
considered because of the lack of age control on
the level of small-scale sedimentary units. The
relative sea level is expressed as:
MS(t) = B a t ( t ) + Sd(t) + Sub(t)
(1)
where MS is the relative sea level at time t, Bat
is paleobathymetry, Sd is the decompacted thickness of sediments deposited until time t and Sub
is the relative position of the underlying sedimentary units and is a function of the total subsidence. All variables are measured in metres.
119
By integrating MS over time, a curve of relative sea-level change during this period is obtained. The curve of relative sea level begins with
the value zero.
The calculations are based on the following
assumptions:
3.1.1. Depositional depth
The water depth has been estimated using the
thickness of oblique stratified oolitic and bioclastic grainstones and comparing sediment composition and faunal evidence to modern sedimentary
environments (Gonzalez, 1993). The height of
sedimentary structures (if enough sediment is
available) is approximately equal or less than one
sixth of the water depth (Allen, 1963; Yalin, 1964;
Jopling, 1966). For sand waves with linear crests
the average water depth is two times the sand
wave height (Rubin and McCulloch, 1980). The
post-depositional erosion of sedimentary structures of ca. 25% (cf. Saunderson and Jopling,
1980; Gonzalez, 1993) and compaction (see below) were taken into account for the water depth
calculations. The water depth of offshoal facies
types was estimated to be in the range of 10-20
m for proximal, non-bioturbated and 15-25 m for
distal, bioturbated tempestites (cf. Howard and
Reineck, 1981; Nelson, 1982; Reineck, 1984; Einsele, 1992). Detailed thin section and facies studies (Trabold, 1990; Allia, 1991; Gonzalez, 1993)
show that possible periods of emergence of the
platform were not preserved.
3.1.2. Subsidence rate
It is assumed that the total subsidence was
constant during the deposition of the Hauptrogenstein Formation because subsidence variations occur less frequently than eustatic variations
(Posamentier et al., 1988). Tectonic activity in
northern Switzerland was probably confined to
well-defined areas during the deposition of the
Hauptrogenstein Formation, as evidenced by
abrupt changes in thickness and facies (Wetzel et
al., 1993; Gonzalez, 1993). The correlation of
sedimentary units shows, that outside these welldefined areas, tectonic movements were not significant. The exact subsidence rate is not known
120
R. Gonzalez / Sedimentary Geology 102 (1996) 111-130
and the value of 30 m Ma-1 has been used as an
example, because this value fits best with subsidence rates calculated by Wildi et al. (1989) and
Loup (1992) and produces a sea-level curve with
moderate relative third-order sea-level changes
(see section 3.3 for more details).
and 80% in micrites (down to 40% after the first
100 m of burial).
3.1.4. Ages
Ages are determined by a re-evaluation of
most of the ammonites found in the last 150 years
in the Hauptrogenstein Formation (Gonzalez,
1993).
3.1.3. Decompaction
Sediments used for interpretation of sea level
were decompacted following data from Matter et
al. (1975), Hamilton (1976), Enos and Sawatsky
(1981), Garrison (1981) and Shinn and Robbin
(1983), assuming an initial porosity of 40-67% for
pack- and grainstones (average porosity 55%,
down to 30% in the first tens of metres of burial,
then changing only slowly), 64-78% in marls
(down to 50-60% after the first 200 m of burial)
3.2. Results
The Schleifenberg section is representative of
the Hauptrogenstein Formation and is used to
illustrate the relative change of sea level calculated from the model presented above. The following discussion is based on the results shown in
Fig. 5.
age
in
~> falling sea-level ma
rising sea-level ,~
biochronozones and
subzones
Spatkalk (only east of
study area; IowstandV
beginning transgressive
systems tract?)
eoa~e~nc~iiieioni~'
__J
~ ,,,.
west; late highstand?)
Movelier Beds (early I
highs?andsystemstract).
"I ....................
"
(transgressivesystems
~tract)
I
] curve of relative ~_
I Lower Oolitic Series
](transgressive systems
roll
[( -r- I
]
~
/ I~
"
I -
]
I
I
'
Lo erAcummata Beds ~
/
/
i
estimatedwater depth
~of sediment deposition
\,
"-,.
................................... hardground
maximum flooding surface
submarine erosion
local hardgrounds
sequence boundary
<
J convergens
[Z r
! !
bomfordi
165.5 1- - -
~
I truelli
~
~
166
acris
5'
i
!
-.
I
166.5 r
garantiana
%~.'I~
" ~ ' ~
167
cuwe of sediment/~
accumulation
considering the
subsidence
167.5
subf.urcatum/
n lortense
i
Rothenflub Beds
(beginning transgressive f~
systemstract/late
16wstand?):
__
I
-----T
blagdeni
168.5 - 168
' 10 ' 20 ~ 30 ' 4 0 ' 50 ' 60
horizons dated with ammonites
marl dominated
offshoal facies
°
wz
164,5
~165
.~ per time unit
_ (decompacted)
/
w
hardground
sequeff~e boundary?
3m
..... ~
=%rac0
!
j ~
_
70 '8(3
DEPTH / THICKNESS (in m)
~
carbonatedominated
platform and rampfacies
Fig. 5. Tentative qualitative evaluation of relative third-order sea-level changes in northern Switzerland during the late Bajocian to
early Bathonian, with an estimated subsidence rate of 30 m M a - 1. Thickness of decompacted sedimentary units and estimation of
depositional depth were taken from the Schleifenberg section. Age data was interpolated from regional values. The absolute ages
were taken from the curve of Haq et al. (1988) in order to make a comparison possible (see Fig. 6). The sequence-stratigraphic
interpretation of lithostratigraphic units is according to the nomenclature reviewed in Van Wagoner et al. (1988). Hardgrounds are
interpreted as maximum flooding surfaces or sequence boundaries.
R. Gonzalez/ Sedimentary Geology 102 (1996) 111-130
From the blagdeni to the acris subzone, a
long-term, slow sea-level rise provided the accommodation space for aggradation and progradation
of bioclastic (Rothenfluh Beds) and later dominantly oolitic platform sediments (Lower Oolitic
Series). These units correspond to a transgressive
systems tract (sensu Van Wagoner et al., 1988).
The sediment production exceeded the accommodation space provided by subsidence and sea-level
rise, leading to the shallowing-up character of the
platform. Surplus sediments were transported
offshore by storms a n d / o r tides. The hardground
at the top of the Lower Oolitic Series marks a
maximum flooding surface (sensu Haq et al., 1988)
and is the end of the first shallowing-up succession.
While the basal sedimentary units could represent late lowstand sediments, an interpretation of
these sediments as prograding lowstand wedge
can be ruled out. A lower sea level would have
been expressed in form of a distinct shallowing
upward trend in the offshoal sediments of the
Klingnau Formation to the east of the Hauptrogenstein Formation, because the subsidence in
this area was near zero (Wildi et al., 1989; Loup,
1992; Gonzalez, 1993). In fact, many sections of
the Klingnau Formation show a deepening-upward trend in beds considered to be coeval with
the base of the Hauptrogenstein Formation. A
shallowing-upward trend is only visible in the
sediments of the upper acris zone, what fits with
the lowstand of sea level during this time as
shown in Fig. 5.
Above the hardground, the marly Upper
Acuminata Beds in the eastern half of the study
area and the Homomya Marls in the western half
of the study area were deposited during the acris
subzone, corresponding to a highstand systems
tract. At this time, ooid production ceased almost
completely, probably because it was outpaced by
sea-level rise. In some sections a deepening-up
succession of marls and tempestites is present in
the first decimeters above the hardground. It is
topped by an ammonite-bearing layer ('Parkinsonien Bank'; Schmassmann, 1945), possibly a
duplication of the maximum flooding surface,
produced by a higher-frequency sea-level change
superimposed on the third-order signal. Above
121
this horizon the marl/tempestite alternations are
again of shallowing-up character. At the top of
the highstand systems tract, a relative sea-level
drop is evidenced by non-deposition or submarine erosion (intensely bioturbated surfaces, local
hardgrounds, erosion marked by channels and
wavy surfaces) and an abrupt vertical change in
facies, replacing offshoal sediments with platform
and ramp sediments. This surface corresponds to
a sequence boundary (Van Wagoner et al., 1988).
Such a submarine erosion of the mostly marly
highstand sediments was possibly produced by
bioerosion and a lowering of the wave base. In
faster subsiding areas in the west of the studied
region, massive, oblique-stratified, bioclastic
grainstones of about 4-5 m thickness overlie the
sequence boundary and correspond to lowstand
deposits in the widest sense. These deposits are,
like at the Schleifenberg section, missing in most
outcrops.
During the following relative rise in sea level
the Upper Oolitic Series were deposited (upper
part of the second shallowing-up succession; upper parkinsoni zone). They are, like their older
counterpart, defined as transgressive systems
tract. Where lowstand deposits appear, a distinction between these and the transgressive systems
tract is often difficult in the field. In many cases,
the transition between lowstand and transgressive
systems tracts is gradual. A distinct transgressive
surface (sensu Haq et al., 1988) is missing.
The hardground on top of the Upper Oolitic
Series marks a marine flooding surface. It is
covered by the marly, bioclastic Movelier Beds
(beginning of the third shallowing-up succession;
beginning of the zig-zag zone, lowest Bathonian),
representing a highstand systems tract. The micritic Coarse Oncolite marks the end of the third
shallowing-up succession in the west and probably represents a late highstand systems tracts.
The switch from a marly (Movelier Beds) to a
micritic matrix (Coarse Oncolite) could have been
caused by a decreased sedimentation of clay particles during the late highstand. The hardground
on top of the Coarse Oncolite is a sequence
boundary. The Spatkalk (which is younger than
the Coarse Oncolite) in the eastern part of the
study area might correspond to a lowstand or
122
R. Gonzalez / Sedimentary Geology 102 (1996) 111-130
transgressive systems tract. These deposits are
missing above the Coarse Oncolite.
3.3. Discussion of third-order sea-leuel change
Curves of third-order sea-level change for the
late Bajocian and earliest Bathonian from Vail et
al. (1984), Haq et al. (1988), Hallam (1988), Rioult et al. (1991) and this paper are compiled in
Fig. 6. All show a moderate sea-level rise during
the late Bajocian and a sea-level maximum during
the parkinsoni zone, which might be a real eustatic signal.
It cannot be said if the development of two
maxima in the Hauptrogenstein Formation instead of one as postulated by all other cited
authors was caused by a eustatic sea-level change
or is the result of a phase of faster subsidence
caused by large-scale, slow tectonic movements.
high sea-levels
Perhaps this apparent discrepancy can be explained by differences in data acquisition (for
example field work vs. seismic), or in the precision of age dating.
The long-term, slow rise in relative sea level,
leading to the creation of new accommodation
space, combined with a moderate subsidence and
a favorable climate is probably responsible for
the creation of unusually thick and widespread
oolitic deposits. In the modern Bahamas for example, the oolitic belt is confined to a relatively
narrow area.
Within the Hauptrogenstein Formation even
at the lowest point of relative sea level, the platform did not emerge (Gonzalez, 1993). It is not
clear why the oolitic shoals in the central barrier
area were not lithified by early cements to form
hardgrounds that would have become emerged
during lowstands. Probably most ooids were
low sea-levels
Lge
n
na
biochronozones and
subzones
163,5
~ y e o v i l e n sNi s ~"1164
o~" I,.,[
164.5
165
165.5
166
166.5
. . . . .
acris
-='
arantiana
O
167
167,5
168
subfurcatum/
niortense 7
[
I [
- : gl
,blagdeni ~
168.5
LSW= Iowstand wedge
TST= transgressivesystems tract
LST= Iowstand systemstract
HST= highstand systemstract
MFS= maximum flooding surface
TS= transgressivesurface
. SB= sequence boundary
third-order sea level fluctuations
Fig. 6. Comparison of the curve of sea-level changes calculated in this paper with other curves presented in the last few years that
cover the same time span. The nomenclature used to classify the sediments formed during certain phases of sea-level change
follows the suggestions of Van Wagoner et al. (1988).
R. Gonzalez/ Sedimentary Geology 102 (1996) 111-130
transported to the eastern outer ramp and to
western platform areas (see also section 4). It
might be speculated that in areas to the east of
the barrier, a relatively high content of very fine
organic material a n d / o r clay particles in the water inhibited the formation of early cements. Remember that the platform and ramp system was
set in a shallow (the order of 50 m deep) epicontinental sea, surrounded by small land areas (e.g.,
Bohemian Massif, Alemannic Land). These underwent constant erosion and produced siliciclastic material that was supplied to the epicontinental sea. However, it must be said that these land
areas were several hundreds of kilometers away
from the study area and an influence is difficult
to prove. West of the oolithic barrier, siliciclastic
influence was minimal. A higher subsidence could
have provided enough accommodation space to
keep the platform constantly submerged.
During strong pulses of sea-level rise the production of shallow-marine carbonates was outpaced and highstand systems tracts were deposited, dominated by marl sediments (and micrites in the Coarse Oncolite). The hardground
on top of the first two shallowing-up successions
do therefore not represent sequence boundaries
with an emersion of the platform, as usually expected. They are instead maximum flooding surfaces, separating transgressive from highstand
systems tracts.
The subsidence rate for the Hauptrogenstein
Formation was probably low in the eastern part
of the study area (near 0 m Ma -1) and about
40-50 m Ma- ~ in the west (Fig. 2; cf. Wildi et al.,
1989; Loup, 1992; Gonzalez, 1993). The subsidence rate used to model the Schleifenberg section was 30 m Ma-a. This is higher than the rates
calculated by Wildi et al. (1989) of 11-25 m
Ma -~. However, they remark that subsidence
rates could have been as high as 40 m Ma -1.
Subsidence rates of 11-25 m Ma -1 would, according to Eq. (1) produce sea-level changes which
are faster and more accentuated than with 30 m
Ma-1. Such high rates of sea-level change seem
improbable for the late Bajocian and earliest
Bathonian, considering the sea-level curves of
other authors (Fig. 6), who all agree, that rates of
sea-level change during this time period were
123
only moderate (cf. Vail et al., 1984; Hallam, 1988;
Haq et al., 1988; Rioult et al., 1991).
4. High-frequency sea-level changes
High-frequency sea-level changes of fourth,
fifth or even higher order have been known for
many years in carbonates, because these sediments express even smallest changes of the environment through facies changes (Fischer, 1964;
Wilson, 1975; Read et al., 1986; Strasser, 1987,
1988). Such high-frequency sea-level changes superimposed on the third-order sea-level changes
(Koerschner and Read, 1989; Goldhammer et al.,
1990; Mitchum and Van Wagoner, 1991). They
produce relatively thin (e.g., Grotzinger, 1986),
shallowing-upward sedimentary successions
('PAC's'--Goodwin and Anderson, 1985; 'parasequences'--Van Wagoner et al., 1988) bounded
by marine flooding surfaces (Mitchum and Van
Wagoner, 1991) and correspond to the small-scale,
shallowing-up units described above.
4.1. Carbonate facies adaptation to fast rises of sea
level: a conceptual model
During most of the time of deposition of the
Hauptrogenstein Formation, shallow-marine,
high-energy conditions prevailed (Fig. 7a). Shifting ooid sand waves appear to have prevented
coral growth. High-energy events (e.g., spring
tides and storms) continuously supplied sediments to deeper offshoal regions and to the platform interior areas,
Fast sea-level rises of moderate amplitude (520 m; 'punctuation events', as postulated by
Goodwin and Anderson, 1985; cf. Grotzinger,
1986) could lead to a period of stagnation and
reorganisation ('lag phase') often marked by erosional features ('marine flooding surfaces'; local
hardgrounds on the platform, erosion on the ramp
during storm events, incision of small channels),
followed by deposition of mud (Fig. 7b). During
these periods, a drop of water energy, combined
with a drop in carbonate concentration prevented
the formation of new ooids. These can only grow
in depths shallower than 5 m, due to the high
Ca 2+ and CO~- concentrations in the water
R. Gonzalez / Sedimentary Geology 102 (1996) 111-130
124
0
km
50
west
east
platform
7a
barrier
ramp
offshoal areas
mean sea-level
s~./waves
/
tides
~dominate
~
storms dominate
_
m
L_ 30
I
7b
new sea-level
former sea-level
15
m
3O
45
-
- ~ -
?oFmer s e a - l e v e l .
.
.
.
.
.
.
.
.
.
.
.
.
.
.
.
.
.
.
.
.
.
.
.
.
.
.
.
.
new sea-level
7c
small buildups
oncoid production
corals
corals
-15
m
'- 30
I
i
L 45
r 0
former sea-level
7d
_ _ -~
-n~wsea~leveF
.
.
.
platform tempestites
small buildups
.
.
.
.
.
// / j
.
.
.
.
.
sand waves
.
.
.
.
.
.
.
.
.
.
.
[
I
i
\
I
~.
' ~ ~ .
offshoal tempestites
15
m
30
45
R. Gonzalez/ Sedimentary Geology 102 (1996) 111-130
needed to form calcite layers on ooids (Simone,
1980).
Subsequently a rich fauna (corals, echinoderms, gastropods, brachiopods, bivalves, etc.)
developed (Fig. 7c), colonizing the substrate above
the marine flooding surfaces. The organisms profited from the absence of shifting ooid sands,
where only a few adapted species (e.g., some
echinoids) can survive (e.g., Meyer, 1988). In addition, many organisms (such as some corals)
produce most carbonates not in the shallowest
water, but in a depth of 20-30 m, due to 'photoinhibition' in the shallowest water (Hottinger,
1984). This is not a contradiction to Schlager's
(1981) statement, that carbonate production fallsoff rapidly below 10 m of depth, because Schlager
(1981) considered total organic carbonate production rates.
Periodically, large storms mixed older ooid
sands with younger bioclastic material. These
storm deposits of extremely heterogeneous content were evenly distributed on the platform in
the form of sand sheets (cf. Ball, 1967). Oncoids
were formed under moderate-energy conditions
in the former area of oolite shoals. In distal areas
marl and clay sedimentation prevailed.
The next period is marked by a stable or a
slightly falling sea level (Fig. 7d). Ooid production began again in shallow areas, as soon as
CaZ+and CO 2- concentrations and water energy
were high enough and increased as the oolite
shoals grew in size. Eventually, oolitic sand waves
prograded and overrode the small coral meadows
and patch reefs.
125
4.2. Discussion of high-frequency sea-level changes
The fact that parasequences show shallowingup tendencies and were deposited under increasing energy practically excludes the possibility of a
climatic control of oolitic vs. non-oolitic periods
[that is, an influx of colder water currents a n d / o r
winds from the north: Fritz (1965) reported a
regional cooling during the Bajocian and Bathonian]. The same is true for control by water
quality (eutrophic vs. oligotrophic conditions;
ooids probably need, like corals, oligotrophic water conditions for growth; cf. Shinn et al., 1990).
However, these factors cannot be excluded for
facies changes within parasequences (e.g., the
complicated hierarchy of oblique stratifications in
sand-wave-dominated parasequences, Fig. 4).
The influence of large-scale tectonic pulses
cannot be easily dismissed as a cause for fast
relative sea-level changes. However, the regularity of intervals in which the ooid production was
interrupted argues against random tectonic pulses
in the Hauptrogenstein Formation.
High-frequency sea-level changes in the Hauptrogenstein Formation can be correlated over several tens of kilometers (Fig. 8); this is usually
considered as an argument for allocyclic control
(e.g., Grotzinger, 1986; Strasser, 1988). The suggestion of Goodwin and Anderson (1985), that
parasequences are produced by fast rises in sea
level, followed by a slow drop in sea level
('punctuation events') appears to fit with the observations made in the Hauptrogenstein Formation. However, it is likely, that the asymmetry of
Fig. 7. Model for facies evolution during small amplitude, high-frequency sea-level changes. The 0.5-6 m thick, small-scale,
shallowing-up sedimentary successions produced correspond to parasequences. (a) Terminal lowstand of sea level. Oolitic
sediments dominate large parts of the platform and ramp realms. Storm sheets are deposited offshoal. (b) Sea-level rise. The
carbonate production is temporarily stopped ('lag phase'). In most areas carbonate mud and clays are deposited, locally
hardgrounds are formed. (c) Beginning 'catch up'. The platform and ramp areas are colonized by corals and other organisms. In
relatively shallow areas oncoids may be formed. On the platform, micritic sediments are deposited. In open, offshoal areas of the
epicontinental sea marl and clay deposition goes on. (d) With a stagnating or slowlysinking sea level, ooid production starts again
in the shallowest areas as soon as carbonate concentrations and water energy are high enough. On the platform, biogenic material
is reworked by storms and deposited in form of platform tempestites. On the ramp, progradation of sand waves begins towards the
offshoal areas. During storms, carbonates are transported offshoal and deposited as offshoal tempestites.
R. Gonzalez / Sedimentary Geology 102 (1996) 111-130
126
c~
•
iili
ii
~<~
i
"
\\
IIII/' ,
'
,,,
/
/ // /
/
\,
\\ /
I
!
/ /
/
/
/
/
,
I
'I
,
I
I~
/
'I
'1,
,,'
,/
'
i
/
,/
//
I
/ //
" /
/ /
/
/
/
,
/
t
/
'
/
~
~q
8
m
5
.o
,6
•~
E
~
"~
E~
g
/ /
oJ
/i
/'
,/
/
i/
/
/
/
/
//
- o ~_~ o oou
oe:~
.
/
/
/
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=
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OO
R. Gonzalez / Sedimentary Geology 102 (1996) 111-130
high-frequency sea-level changes is accentuated
by (1) subsidence and (2) the 'lag' phase in carbonate production during high rates of sea-level
rise. This effect overemphasises sediments produced during the subsequent 'catch-up' phase of
a parasequence in the sedimentary record. The
time span represented by erosional surfaces and
following tempestite and bioclastic deposits is
longer than the time span represented by thick
oolitic grainstone deposits.
There is no point in trying to correlate the
small-scale sequences to cyclicities, as postulated
by Milankovitch (1941) or Hays et al. (1976),
because:
(1) There is absolutely no age control. In tidal
sediments there is a large lateral variance of bed
thickness. Sedimentary units with a thickness of
several metres in one section can laterally disappear and be only represented as 'lag' in other
sections.
(2) It is impossible to say if and how many
cycles have been completely removed by submarine erosion. Probably only sediments produced
during a rising or stable sea level were preserved.
(3) The formation of parasequences was probably influenced by various, superimposed cyclicities. Most parasequences may have originated
from 100 ka cycles, but others may have a strong
40 or 20 ka cycle influence. Again, the lack of age
control makes it impossible to produce a reasonable interpretation.
(4) The influence of other control factors for
carbonate production (water quality, climate, tectonics) is not well understood and might be responsible for much of the 'noise' of sedimentation/erosion patterns within the Hauptrogenstein Formation.
127
5. Conclusions
The Hauptrogenstein Formation of northern
Switzerland (late Bajocian to earliest Bathonian)
records the effects of sea-level changes and subsidence. Vertical facies changes are used to determine sea-level fluctuations of third-order and
higher-frequency sea-level changes (below biostratigraphic resolution).
A maximum of sea level at the top of the
Bajocian with the development of two sea-level
highstands is observed in the Hauptrogenstein
Formation, instead of one as postulated by Vail
et al. (1984), Haq et al. (1988), Hallam (1988) or
Rioult et al. (1991) in other parts of Western
Europe.
Strong pulses of sea-level rise outpaced the
production of shallow-marine carbonates and the
highstand systems tracts at the base of the second
and in the third shallowing-up successions were
deposited. The platform-wide hardgrounds on top
of the first two shallowing-up successions do not
represent sequence boundaries with an emersion
of the platform. They are major marine flooding
surfaces, separating transgressive and highstand
systems tracts. The hardground on top of the
third shallowing-up succession (top of the Hauptrogenstein Formation) is a sequence boundary.
The lack of intra- and supratidal sediments
and cements during lowstands in the eastern part
of the study area may be due to a relatively high
content of fine organic and siliciclastic material in
the water, which inhibited the formation of early
cements and the stabilisation of sediments. In the
west a higher subsidence may have provided
enough accommodation space to keep the platform constantly submerged.
Fig. 8. West-east correlation of part of a few studied sections (see Fig. 1 for localisation), showing the uppermost parasequences of
the Lower Oolitic Series, the Upper Acuminata Beds, respectively, the Homomya Marls and the basal Upper Oolitic Series. This
part of the Hauptrogenstein Formation is a good example for the transition from transgressive to highstand and back to
transgressive systems tracts in the platform and ramp environments. Local environmental (water energy, currents) and external
control factors (subsidence variations) are responsible for the lateral variation of the parasequences. This is best seen in the fast
lateral transition from platform facies (Upper Acuminata Beds and Upper Oolitic Series) at Cballpass to offshoal facies (Homomya
Marls) at Liesberg, due to an increased tectonic subsidence at and west of Liesberg.
128
R. Gonzalez / Sedimentary Geology 102 (1996) 111-130
Within the three major shallowing-up successions, small-scale, high-frequency, allocyclic sealevel changes are well documented in form of
facies changes. Parasequences usually show three
vertical phases of development: (1) a more or less
thick layer of marls and clays, poor in sand-sized
components and deposited during low-energy periods; (2) carbonates dominated by biogenous/
bioclastic material in the widest sense (including
oncoids), deposited under moderate-energy conditions with episodic high-energy events (storms):
(3) high-energy, tidal sand waves dominated by
ooids.
Acknowledgements
Thanks to A. Wetzel for long discussions and
field trips. I am indebted to G. Dietl (Staatliches
Museum fiir Naturkunde, Stuttgart, Germany),
who, in an incredible tour de force, re-evaluated
over 200 ammonites. Saluti to D. Bernoulli, G.
Eberli and A. Strasser who helped me a lot in
understanding the fundamentals of sequence
stratigraphy. Useful and constructive reviews were
provided by R. Leinfelder, M. Tucker and A. van
de Weerd. Thanks to Cam Davidson for improving my English. Financial support was provided
by the Swiss National Science Foundation (Grants
No. 20-31227.89 and 20-31227.91).
References
Allen, J.R.L., 1963. Asymmetrical ripple marks and the origin
of water-laid cosets of cross-strata. Liverpool Manchester
Geol. J., 3: 187-236.
Allen, J.R.L., 1980. Sand waves: A model of origin and
internal structures. Sediment. Geol., 26: 281-328.
Allen, J.R.L., 1984. Sedimentary Structures, their Character
and Physical Basis. Unabridged one-volume edition. (Developments in Sedimentology, 30) Elsevier, Amsterdam,
1256 pp.
Allen, P.A. and Allen, J.R.L., 1990. Basin Analysis, Principles
and Applications. Blackwell, Oxford, 451 pp.
Allia, V., 1991. Bildung und Diagenese yon Hartgriinden im
Hauptrogenstein (mittlerer Dogger) in der NW-Schweiz.
M. Thesis, Univ. Basel (unpubl.),
Ball. M.M., 1967. Carbonate sand bodies of Florida and the
Bahamas. J. Sediment. Petrol., 37: 556-591.
De Mowbray, T. and Visser, M.J., 1984. Reactivation surfaces
in subtidal channel deposits, Oosterschelde, SW Netherlands. J. Sediment. Petrol., 54: 811-824.
Droxler, A.W., Schlager, W. and Whallon, C.C., 1983. Quaternary aragonite cycles and oxygen-isotope record in Bahamian carbonate ooze. Geology, 11: 235-239.
Eberli, G.P. and Ginsburg, R.N., 1989. Cenozoic progradation
of northwestern Great Bahama Bank, a record of lateral
platform growth and sea level fluctuations. Soc. Econ.
Paleontol. Mineral., Spec. Publ., 44: 339-351.
Einsele, G., 1992. Sedimentary Basins. Evolution, Facies and
Sediment Budget. Springer, Berlin.
Enos, P. and Sawatsky, L.H., 1981. Pore networks in Holocene
carbonate sediments. J. Sediment. Petrol., 51: 961-985.
Fischer, A.G., 1964. The Lofer cyclothems of the Alpine
Triassic. Bull. Kans. State Geol. Surv., 169: 107-149.
Fritz, P., 1965. 180/160-Isotopenanalysen und Paliiotemperatur-bestimmungen an Belemniten aus dem schwiibischen
Jura. Geol. Rundsch., 54: 261-269.
Garrison, R.E., 1981. Diagenesis of oceanic carbonate sediments: a review of the DSDP perspective. Soc. Econ.
Paleontol. Mineral. Spec. Publ., 32: 181-207.
Goldhammer, R.K., Oswald, E.J. and Dunn, P.A., 1990. Forward modeling of high-frequency, depositional sequences:
an example from Middle Pennsylvanian shelf carbonates
of the SW Paradox Basin, Honnacker Trail, Utah. Abstr.
Am. Assoc. Pet. Geol. Bull., 74: 663.
Gonzalez, R., 1993. Die Hauptrogenstein-Formation der
Nordschweiz (mittleres Bajocien bis unteres Bathonien).
Ver6ff. Geol. Paliiontol. Inst. Basel 2.
Goodwin, P.W. and Anderson, E.J., 1985. Punctuated aggradational cycles: a general hypothesis of episodic stratigraphic accumulation. J. Geol., 93(5): 515-533.
Grotzinger, J.P., 1986. Cyclicity and paleoenvironmental dynamics, Rocknest platform, northwest Canada. Bull. Geol.
Soc. Am., 97: 1208-1231.
Hallam, A., 1975. Jurassic Environments. Cambridge Univ.
Press, Cambridge, 269 pp.
Hallam, A., 1988. A reevaluation of Jurassic eustacy in the
light of new data and the revised Exxon curve. In: C.K.
Wilgus, B.S. Hastings, C.A. Ross, H. Posamentier, J. van
Wagoner and C.G.St.C. Kendall (Editors), Sea-level
Changes: An Integrated Approach. Soc. Econ. Paleontol.
Mineral., Spec. Publ., 42: 261-273.
Hamilton, E.L., 1976. Variations of density and porosity with
depth in deep-sea sediments. J. Sediment. Petrol., 46:
280-300.
Harms, J.C., Southard, J.B. and Walker, R.G., 1982. Structures and sequences in clastic rocks. Soc. Econ. Paleontol.
Mineral. Short Course 9.
Haq, B.U., Hardenbol, J. and Vail, P.R., 1988. Mesozoic and
Cenozoic chronostratigraphy and eustatic cycles. In: C.K.
Wilgus, B.S. Hastings, C.A. Ross, H. Posamentier, J. van
Wagoner and C.G.St.C. Kendall (Editors), Sea-level
Changes: An Integrated Approach. Soc. Econ. Paleontol.
Mineral., Spec. Publ., 42: 71-108.
Hays, J.D., Imbrie, J. and Shackleton, N.J., 1976. Variations
R. Gonzalez/ Sedimentary Geology 102 (1996) 111-130
in the Earth's orbit: pacemaker of the ice ages. Science,
194: 1121-1132.
Hottinger, L., 1984. Strat6gies vitales et processus 6coiogiques
selectionn6s r6gissant la constitution de corps bioconstructifs. In: J. Geister and R. Herb (Editors), G6ologie et
Pal6oecologie des R6cifs. 3~me Cycle Romand en Sciences
de la Terre, Univ. Bern.
Houthhuys, R. and Gullentops, F., 1988. Tidal transverse bars
building up a longitudinal sand body (Middle Eocene,
Belgium). In: P.L. de Boer, A. van Gelder and S.D. Nio
(Editors), Tide-Influenced Sedimentary Environments and
Facies. Reidel, Dordrecht, pp. 153-166.
Howard, J.D. and Reineck, H.E., 1981. Depositional facies of
high-energy beach-to-offshore sequence: Comparison with
low energy sequence. Am. Assoc. Pet. Geol. Mineral.
Bull., 85: 807-830.
Javaux, C., 1992. La plate-forme Parisienne et Bourgignonne
au Bathonien et au Callovien: dynamique s6dimentaire,
s6quentielle et diag6n6tique. Place et cr6ation des
r6servoirs potentiels. M6m. G6ol. Univ. Dijon 16, 342 pp.
Jopling, A.V., 1966. Some principles and techniques used in
reconstructing the hydraulic parameters of a paleo-flow
regime. J. Sediment. Petrol., 36: 5-49.
Koerschner III, W.F. and Read, J.F., 1989. Field and modelling studies of Cambrian carbonate cycles, Virginia Appalachians. J. Sediment. Petrol., 59: 654-687.
Loup, B., 1992. Mesozoic subsidence and stretching models of
the lithosphere in Switzerland (Jura, Swiss Plateau and
Helvetic realm). Eclogae Geol. Helv., 85(3): 541-572.
Matter, A., Douglas, R.G. and Perch-Nielsen, K., 1975. Fossil
preservation, geochemistry and diagenesis of pelagic carbonates from Shatsky Rise, northwest Pacific. In: J.V.
Gardner (Editor), Initial Reports of the Deep Sea Drilling
Project. U.S. Gov. Print. Off., pp. 891-921.
McCabe, P.J. and Jones, C.M., 1977. Formation of reactivation surfaces within superimposed deltas and bedforms. J.
Sediment. Petrol., 47: 707-715.
Meyer, C., 1988. Pal~io6kologie, Biofazies und Sedimentologie
yon Seeliliengemeinschaften aus dem Unteren Hauptrogenstein der Nordwestschweizer Jura. Rev. Pal6obiol., 7(2):
359-433.
Milankowitch, M., 1941. Kanon der Erdbestrahlung und seine
Anwendung auf das Eiszeitenproblem. Acad. R. Serbe
Spec. Ed. 133, 633 pp.
Mitchum, R.M. and Van Wagoner, J.C., 1991. High-frequency
sequences and their stacking patterns: sequence-stratigraphic evidence of high-frequency eustatic cycles. Sediment. Geol., 70: 131-160.
Miihlberg, M., 1900. Die Stratigraphie des braunen Jura im
nordwestschweizerischen Juragebirge. Eclogae Geol. Helv.,
6(4): 293-332.
Nelson, C.H., 1982. Modern shallow-water graded sand layers
from storm surges, Bering shelf: a mimic of Bouma-sequences and turbidite systems. J. Sediment. Petrol., 52:
537-545.
Posamentier, H.W., Jervey, M.T. and Vail P.R., 1988. Eustatic
controls on clastic deposition I--conceptual framework.
In: C.K. Wilgus, B.S. Hastings, C.A. Ross, H. Posamentier,
129
J. van Wagoner and C.G.St.C. Kendall (Editors), Sea-level
Changes: An Integrated Approach. Soc. Econ. Paleontol.
Mineral., Spec. Publ., 42: 109-124.
Read, J.F., Grotzinger, J.P., Bova, J.A. and Koerschner, W.F.,
1986. Models for generation of carbonate cycles. Geology,
14: 107-110.
Reijmer, J.J.G., Schlager, W. and Droxler, A.W., 1988. Site
632: Pliocene-Pleistocene sedimentation in a Bahamian
basin. Proc. ODP, Sci. Results, 101: 213-220.
Reineck, H.-E., 1984. Aktuogeologie klastischer Sedimente.
Waldemar Klein, Frankfurt.
Rioult, M., Dugu6, O., Jan du Chine, R., Ponsot, C., Fily, G.,
Moron, J.-M. and Vail, P.R., 1991. Jurassic outcrop sequence stratigraphy of Normandy. Bull. Cent. Rech. Explor. Prod. Elf Aquitaine, 15(1): 101-194.
Rubin, D.M. and McCulloch, D.S., 1980. Single and superimposed bedforms: A synthesis of San Francisco Bay and
flume observations. Sediment. Geol., 26: 207-231.
Sarg, J.F., 1988. Carbonate sequence stratigraphy. In: C.K.
Wilgus, B.S. Hastings, C.A. Ross, H. Posamentier, J. van
Wagoner and C.G.St.C. Kendall (Editors), Sea-level
Changes: An Integrated Approach. Soc. Econ. Paleontol.
Mineral., Spec. Publ., 42: 155-182.
Saunderson, H.C. and Jopling, A.V., 1980. Paleohydraulics of
a tabular cross-stratified sand in the Brampron Esker,
Ontario. Sediment. Geol., 25: 169-188.
Schlager, W., 1981. The paradox of drowned reefs and carbonate platforms. Geol. Soc. Am. Bull., 92: 197-211.
Schlager, W., 1992. Sedimentology and sequence stratigraphy
of reefs and carbonate platforms. Am. Assoc. Pet. Geol.
Contin. Educ. Course Note Ser. 34.
Schmassmann, H.J., 1945. Stratigraphie des mittleren Doggers
der Nordschweiz. T~itigkeitsber. Naturforsch. Ges. Baselland 14.
Shinn, E.A. and Robbin, D.M., 1983. Mechanical and chemical compaction in fine-grained shallow-water limestones. J.
Sediment. Petrol., 53: 595-618.
Shinn, E.A., Lidz, B.H. and Holmes, C.W., 1990. High-energy
carbonate-sand accumulation, the Quicksands, southwest
Florida. J. Sediment. Petrol., 60(6): 952-967.
Simone, L., 1980. Ooids: A review. Earth Sci. Rev., 16:
319-355.
Strasser, A., 1987. Detaillierte Sequenzstratigraphie und ihre
Anwendung: Beispiel aus dem Purbeck des schweizerischen und franz6sischen Jura. Facies, 17: 237-244.
Strasser, A., 1988. Enregistrement s6dimentaire de cycles
astronomiques dans le Portlandien et Purbeckien du Sal~ve
(Haute-Savoie, France). Arch. Sci. Gen~ve, 41(1): 85-97.
Trabold, G., 1990. Mikrofazielle und diagenetische Entwicklung des Unteren und Mittleren Hauptrogenstein im
siidlichen Rheingraben. Unpubl. M. Thesis, Univ. Heidelberg.
Vail, P.R., Mitchum Jr., R.M. and Thompson III, S., 1977a.
Relative changes of sea-level from coastal onlap. In: C.E.
Payton (Editor), Seismic Stratigraphy--Applications to
Hydrocarbon Exploration. Am. Assoc. Pek Geol. Mere.,
26: 63-82.
Vail, P.R., Mitchum Jr., R.M. and Thompson III, S., 1977b.
130
R. Gonzalez / Sedimentary Geology 102 (1996) 111-130
Seismic stratigraphy and global changes of sea-level, Part
4: Global cycles of relative changes of sea-level. In: C.E.
Payton (Editor), Seismic Stratigraphy--Applications to
Hydrocarbon Exploration. Am. Assoc. Pet, Geol. Mem.,
26: 83-97.
Vail, P.R., Hardenbol, J. and Todd, R.G., 1984. Jurassic
unconformities, chronostratigraphy and sea-level changes
from seismic stratigraphy and biostratigraphy. In: J.S.
Schlee (Editor), Interregional Unconformities and Hydrocarbon Accumulation. Am. Assoc. Pet. Geol. Bull., 36:
129-144.
Vail, P.R., Colin, J.-P., Du Chene R.J., Kuchly, J., Mediavilla,
F. and Trifilieff, V., 1987. La stratigraphie s6quentielle et
son application aux corr61ations chronostratigrapbiques
dans le Jurassique du bassin de Paris. Bull. Soc. G~.ol. Fr.,
(8), 3(7): 1301-1321.
Van Wagoner, J.C., Posamentier, H.W., Mitchum Jr., R.M.,
Vail, P.R., Sarg, J.F., Loutit, T.S. and Hardenbol, J., 1988.
An overview of the fundamentals of sequence stratigraphy
and key definitions. In: C.K. Wilgus, B.S. Hastings, C.A.
Ross, H. Posamentier, J. van Wagoner and C.G.St.C.
Kendall (Editors), Sea-level Changes: An Integrated Approach. Soc. Econ. Paleontol. Mineral., Spec. Publ., 42:
39-46.
Wetzel, A., Allia, V., Gonzalez, R. and Jordan, P., 1993.
Sedimentation und Tektonik im Ostjura. Eclogae Geol.
Helv., 86(1): 313-332.
Wildi, W., Funk, H., Loup, B., Amato, E. and Huggenberger,
P., 1989. Mesozoic subsidence history of the European
marginal shelves of the alpine Tethys (Helvetic, Swiss
Plateau and Jura). Eclogae Geol. Helv., 82: 817-840.
Wilson, J.L., 1975. Carbonate Facies in Geologic History.
Springer, Berlin, 471 pp.
Yalin, M.S., 1964. Geometrical properties of sand waves.
Proc. Am. Soc. Civil Eng. J. Hydraul. Div., 90: 105-119.