The Jurassic of the Netherlands
G.F. Waldemar Herngreen, Wim F.P. Kouwe and Theo E.Wong
A recent revision of the lithostratigraphy of the Netherlands has triggered an extensive re-evaluation of existing ideas on the Jurassic structural and depositional history. Significant advances
can be attributed to the incorporation of sequence stratigraphic concepts. In the course of the
Triassic and Jurassic, structural complexity increased progressively. The Jurassic sedimentary succession can be subdivided into three depositional megasequences. Megasequence I (Rhaetian–
Aalenian) reflects the period between the so-called early and mid-Cimmerian tectonic phases.
Megasequence II (Aalenian – Middle Callovian) covers the period of activity of the mid-Cimmerian
phase. Megasequence III (Middle Callovian – Ryazanian) corresponds with the period between
the mid-Cimmerian and late Cimmerian phases (particularly after pulse II). In this latter megasequence, six stages (IIIa–f) are recognised. Sediments deposited during the Rhaetian and Ryazanian
bear a stronger affinity with the Jurassic succession than with Triassic and Cretaceous sediments
respectively. These stages are thus treated here as an integral part of the Jurassic succession. During
the Rhaetian–Bajocian the area subsided relatively uniformly. A sheet of predominantly fine-grained
marine sediments of great lateral uniformity was deposited. During the Toarcian, in particular,
basin circulation was largely restricted.
The cooling that followed the thermal Central North Sea dome uplift triggered an important
extensional phase during the Aalenian–Callovian. The rift phase resulted in the formation of several smaller basins, each with its own characteristic depositional succession. The basins fall into
three structural provinces: the eastern province (Lower Saxony Basin, E–W-striking); the northern
province (Central Graben, N–S-striking); and the southern–central system (Roer Valley Graben –
Broad Fourteens, with a strong NW–SE strike). The mid-Cimmerian event started to affect the
Dutch basins during the Bajocian. Sedimentation ceased in the Dutch Central Graben while it
persisted in a predominantly coarse-grained, shallow marine facies in the southern basins (Roer
Valley Graben, West Netherlands Basin). Extensional tectonics in the Central Graben were initiated during the Middle Callovian, with the deposition of continental sediments. During the
Oxfordian–Kimmeridgian, marine incursions gradually became more frequent. Marine deposition in the other basins in the south persisted into the Oxfordian, at which time deposition
became predominantly continental. Marine conditions gradually returned in the south during the
Ryazanian–Barremian, with a series of advancing partial transgressions from the north. The present-day distribution of Jurassic strata in the Netherlands was determined largely by erosion associated with Late Cretaceous – Paleocene uplift.
Keywords: The Netherlands onshore and offshore, Jurassic, lithostratigraphy, sequence stratigraphy, tectonics,
regional geology
G.F.W.H.* & T.E.W., Netherlands Institute of Applied Geoscience TNO – National Geological Survey, P.O. Box 80015,
NL-3508 TA Utrecht, The Netherlands. *Retired. E-mail: [email protected]
W.F.P.K., Wintershall Noordzee B.V., Eisenhowerlaan 146, NL-2517 JL The Hague, The Netherlands.
Geological Survey of Denmark and Greenland Bulletin 1, 217–229 (2003)
© GEUS, 2003
217
The Jurassic succession in the Netherlands has significant hydrocarbon source rock and reservoir potential
and the stratigraphy of the succession is thus a subject
of particular interest. The Jurassic lithostratigraphic
nomenclature in the Netherlands has recently been
updated in a joint effort by the Geological Survey of
the Netherlands (RGD) and NOGEPA, the organisation
of oil companies active in the Netherlands. This project has benefited significantly from integration of new
knowledge on Jurassic biostratigraphy. In addition,
sequence stratigraphic concepts have been used to
explain the observed distribution of facies in time and
space. The results have been published in part in van
Adrichem Boogaert & Kouwe (1994–1997). In this study,
we treat the most recent ideas about the Jurassic geological history of the Netherlands.
The geological history of the Jurassic in the Netherlands has been presented previously by Haanstra (1963),
Heybroek (1974) and van Wijhe (1987). Ziegler (1990)
treated the area from a Northwest European perspective, whereas Burgers & Mulder (1991) summarised certain aspects of the Late Jurassic and Cretaceous history.
Regional stratigraphic overviews of the Jurassic in the
southern North Sea have been presented by Brown
(1990) and Cameron et al. (1992). Michelsen & Wong
(1991) presented a stratigraphic correlation between
the Dutch, Danish and southern Norwegian sectors of
the Central Graben. Underhill & Partington (1993) discussed the effect of Middle Jurassic thermal doming on
regional Jurassic stratigraphy in a sequence stratigraphic
context. Kimmeridgian to Ryazanian sequence stratigraphy, biostratigraphy and the distribution of the main
reservoir intervals in the North Sea were dealt with by
Partington et al. (1993).
During the last two decades, several authors from the
Geological Survey of the Netherlands (RGD) have published detailed review papers on the Middle–Late Jurassic
history of the Dutch Central (North Sea) Graben, the
Vlieland Basin and adjoining onshore areas: Herngreen
& de Boer (1984), Herngreen & Wong (1989), Herngreen
et al. (1988, 1991), Wong et al. (1989), Geological Atlas
of the Subsurface of the Netherlands, sheets I–V (RGD
1991a, b, 1993a, b, 1995) and X (NITG–TNO 1998; map
sheet VI is in press and sheets VII and VIII are currently
in preparation).
The accumulated RGD knowledge, combined with
contributions by several oil companies, served as a
basis for the revision of the existing lithostratigraphic
nomenclature for the Netherlands (van Adrichem
Boogaert & Kouwe 1994–1997). The revision of the
Jurassic involved two working groups: Permian – Middle
218
Jurassic and Upper Jurassic – Lower Cretaceous. A correlation of the current Dutch Jurassic – Lower Cretaceous
lithostratigraphy with the stratigraphic subdivisions of
the neighbouring countries is presented in Figure 1.
Structural setting
During Triassic–Jurassic times, the structural style of the
Netherlands gradually changed from the single, extensive
Southern Permian Basin into a complex of smaller, largely
fault-controlled, highs and lows. This transformation,
related to the break-up of Pangea (Ziegler 1990), took place
in several discrete extensional phases: Scythian (Hardegsen), Norian–Rhaetian (early Cimmerian), Aalenian –
Callovian/Oxfordian (mid-Cimmerian) and Kimmeridgian–
Valanginian (late Cimmerian). The intervening periods
were dominated by regular thermal subsidence.
The result can be seen by comparing Figures 2 and 3,
which display the Triassic and Late Jurassic basin configurations, respectively. In the northern half of the
Netherlands’ offshore territory, the segregation between
highs and basins was enhanced by halokinesis in the
Permian–Triassic successions along the structural boundaries. Associated salt withdrawal commonly determined
the distribution of Jurassic depocentres.
Throughout the Jurassic, the area comprised three
interactive structural provinces (Fig. 3).
1. The Lower Saxony Basin system (previous Ems Low),
extending into central Germany.
2. The North Sea Central Graben – Vlieland Basin system, trending north–south across the Mid-North Sea
High – Ringkøbing–Fyn High complex.
3. A block-faulted basin system extending NW–SE
through the Netherlands, connecting the Roer Valley
Graben, the Central Netherlands Basin, the West
Netherlands Basin and the Broad Fourteens Basin
(previous Off-Holland Low), and linked with the
Sole Pit Basin in the UK offshore.
During the Early Jurassic, the area subsided relatively
uniformly. A sheet of open marine, fine-grained sediments of great lateral uniformity was deposited. Structural
complexity gradually increased during Early and Middle
Jurassic times, and reached a maximum in the Callovian.
During the Middle and Late Jurassic, in particular, each
of the above-mentioned provinces accumulated its own
characteristic depositional succession.
The impact of the uplift of the Central North Sea
thermal dome during the Aalenian–Bathonian is most
219
?
= hiatus
Winterton Fm
Oxford Clay Fm
Corallian Fm
Kimmeridge Clay Fm
Spilsby
Sandstone
Fm
Speeton Clay Fm
Vlieland
Sandstone
Fm
Sleen Fm
Aalburg Fm
Upper
Graben
Fm
Lower Graben Fm
Middle Graben Fm
Puzzle
Hole
Fm
Posidonia Shale Fm
Werkendam Fm
Brabant Fm
Friese
Front
Fm
Kimmeridge
Clay Fm
Scruff
Greensand Fm
Vlieland Claystone Fm
Holland Fm
Winterton Fm
?
Heno
Fm
Poul
Fm
Vyl
Fm
Bryne Fm
Fjerritslev Fm
Lower
Graben
Sand
Fm
Middle Graben
Shale Fm
Lola Fm
Farsund Fm
Valhall Fm
Tuxen Fm
Sola Fm
Rødby Fm
source: Jensen et al. (1986),
Michelsen & Wong (1991)
Denmark
Danish Central Graben
Altena Group
Nieuwerkerk Fm
Delfland Subgroup
Epoch
Sleen Fm
Aalburg Fm
Posidonia Shale Fm
Werkendam Fm
Weiteveen Fm
Coevorden Fm
Vlieland
Sandstone
Fm
Vlieland
Claystone
Fm
Holland Fm
Netherlands
(north-)eastern sector
Rhätkeuper
Posidonienschiefer
‘Cornbrash’
WürttembergicusSandstein
AspidoidesSandstein
Porta-Sandstein
(Macroceph. sst)
Macrocephalenton
Wiehengeb.Korallenquarzit
oolith
Heersumer Schichten
Ornatenton
Münder Fm
Eimbeckhäuser Plattenkalk
Gigasschichten
Kimmeridgekalke & -mergel
Serpulit Mb
Bückeberg Fm (‘Wealden’)
Bentheimer
Sandstein
Gildehäuser
Sandstein
Neokom-Schieferton
(Hilston Fm)
RothenbergSandstein
source: Brinkmann (1959),
Casey et al. (1975),
Kemper(1976), Klassen (1984)
Flammenmergel
Minumuston
Osning grønsand
Germany
Lower Saxony Basin
(western part)
Fig. 1. Regional lithostratigraphic correlation chart of the Jurassic – Lower Cretaceous for the Netherlands and neighbouring countries. Kimmeridgian sensu lato equals Kimmeridgian
sensu anglico. For recent revisions of the Danish scheme, see Michelsen et al. (2003, this volume). Modified from van Adrichem Boogaert & Kouwe (1994–1997).
Rhaetian
Hettangian
Sinemurian
Pliensbachian
Toarcian
Aalenian
Bajocian
Bathonian
Callovian
Oxfordian
Kimmeridgian
(sensu lato)
Portlandian
Ryazanian
Valanginian
Hauterivian
Barremian
Aptian
Red Chalk Fm
Breeveertien Fm
Albian
Zurich Fm
source: Rhys (1974),
Cameron et al. (1992)
Netherlands
composite for the northern,
central and western sectors
Cromer Knoll Group
Central Graben Gp
United Kingdom
Southern North Sea
Rijnland Group
Niedersachsen Gp
Osningsandstein
Age
Schieland Group
Altena Group
Early Cretaceous
Late Jurassic
Middle Jurassic
Early Jurassic
L. Triassic
Rijnland Group
Scruff Group
Central Graben
Subgroup
Cromer Knoll Group
Humber Group
West Sole Group
Lias Group
Penarth
Group
Malm
Dogger
Lias
Keuper
Ringkøbing–Fyn
High
A
4
5
7
9
12
13 14
15
R if g
Cleaver Bank
High
M
54°N
N
K
fat
iga
bl
P
ow
ne
Ems L
zo
es
t
N
e
Ba the
sin rla
n
O
R S
lt
W
Winterton
High
52°N
es
nd
vo
Ce
or
ntr
tR
idg
tN
Ba ethe
sin rla
n
e
ro
na
u
fau
lt
zo
ne
Maasbommel
High
dH
igh
Rhenish Massif
G
al N
e
Bas therl
and
in
s
l
efe
G
Platform/occasionally flooded
Lower Saxony
Basin
Gouwzee
Trough
ck
DK
ne
Friesland
Platform
l–I
or
Js
d
Pla –Ho Hig selm
ee
h
tfo lla
r
n
rm d
London–Brabant
Massif
3°E
zo
Kr
7°E
Structural high/subaerial landmass
N
Q
IJmuiden
High
lt
Blo
5°E
fau
el
3°E
m
Pe
London–Brabant
Massif
ntu
y
lle
Va n
er abe
Ro Gr
Ro
e
Gr r V
ab alle
en y
N
xe
ds
ds
e
Ameland
Block
Ha
Te
No
Za
O
R S
zon
Vlieland
Basin
W
East Netherlands
High
fa u lt
Terschelling
Basin
fau
South
Hewett
Shelf
Broad
Fourteens
Basin
e
Q
den
Vlieland
High
de
Netherlands
Swell
18
Schill Grund
High
ron
M
L
Sole Pit
Basin
Off-Holland
Low
NL
en
Centr
G
In
8
10 11
UK
100 km
G
6
16 17
P
52°N
F
en
ng
ni h
ro ig
G H
ee
sz
er gh
uw u
La Tro
Sole Pit
Basin
3 L
2
E
100 km
al Gra
b
F
raben
B
Central
K1
Ringkøbing–Fyn
High
Step G
ig h
it H
Sp
54°N
Outer
Rough
Basin
it
Sp
ow h
Elb Hig
ow
E lb
E
A
Mid North Sea
High
B
Graben
Mid North
Sea High
Rhenish
Massif
5°E
7°E
Fig. 3. Middle–Late Jurassic to Early Cretaceous structural elements
in the Netherlands. For legend, see Fig. 2. Modified from van
Adrichem Boogaert & Kouwe (1994–1997).
Basin
Major normal fault (zone)
Seismic line shown in Fig. 6
Fig. 2. Main Triassic to Early Jurassic structural elements in the
Netherlands. The K-quadrant shows the block numbering system
used for the Netherlands’ continental shelf. Each complete quadrant (1°N x 1°E) is divided into 18 blocks measuring 10´N x 20´E,
numbered from NW to SE. Incomplete quadrants are numbered
as if they were complete (e.g. the O-quadrant only comprises
blocks 12, 15, 17 and 18). National sectors of the North Sea: DK,
Denmark; G, Germany; N, Norway; NL, the Netherlands; UK,
United Kingdom. Modified from van Adrichem Boogaert & Kouwe
(1994–1997).
evident in the northern offshore area of the Netherlands,
where Lower Jurassic successions are deeply truncated.
The combination of initial cooling of the thinned crust
under the dome and an overall transtensional tectonic
220
regime triggered Callovian–Kimmeridgian rifting, resulting in the formation of the North Sea Central Graben
rift system.
The uplift phase terminated the uniform subsidence
and sheet-like deposition that characterised the Early
and Middle Jurassic. Rifting induced structural differentiation into rapidly subsiding basins with high sediment infill rates and more stable, sediment-starved,
platform areas. This differentiation persisted until the
Early Cretaceous. Outside the main basins depicted in
Figure 3, Upper Jurassic deposits are rare and thin, and
associated with salt domes (rim synclines) or transverse
fault zones.
The north-eastern part of the Netherlands formed the
western fringe of the German Ems Low – Lower Saxony
Basin system. The Ems Low, a north–south elongated,
fault-bounded basin during Carboniferous–Triassic times,
evolved into the slightly east–west-trending, sag-like
Lower Saxony Basin during the Middle Jurassic. A relatively undisturbed, continuous Jurassic succession is
found in the central parts of the basin in Germany (Fig.
1). In the eastern Netherlands’ development, a hiatus
spanning the Aalenian – Early Kimmeridgian reflects the
situation along the western margin of the basin.
The West Netherlands Basin, the Roer Valley Graben
and the Broad Fourteens Basin formed a different depositional province, connected with the Sole Pit Basin of
the UK sector of the North Sea. Since Permian–Triassic
salts are largely absent in the subsurface here, these
basins demonstrate a pure block-faulted nature. The
three mentioned provinces merge in the onshore
Netherlands, where the Central Netherlands Basin and
the Vlieland Basin (a small pull-apart basin) were positioned. The transitions between these provinces are
now obscured as a result of later erosion which has
stripped Jurassic sediments from most of the country.
Application of sequence stratigraphy
In connection with the revision of the existing lithostratigraphic nomenclature for the Netherlands (van
Adrichem Boogaert & Kouwe 1994–1997), sequence
stratigraphic analysis was seen as a valuable additional
tool for a better understanding of the complex geological settings and stratigraphic relationships. The
Lower and Middle Jurassic successions in the Netherlands
are of open marine origin, and developed in regionally uniform facies. Depositional cycles are commonly
discerned in this interval, and some of these were
already incorporated in the old lithostratigraphic subdivision by NAM & RGD (1980). In the recent revisions,
therefore, it was not considered necessary to improve
this scheme by incorporation of results from new biostratigraphic or sequence stratigraphic analyses. In the
(Middle–)Upper Jurassic, however, the common intercalation of continental and marine deposits makes
sequence stratigraphy especially effective. Therefore
all available data (well and seismic correlations, biostratigraphic and palynological data) were integrated into
a regional sequence stratigraphic framework. This framework was used to select those units which were suitable candidates for lithostratigraphic units. Criteria for
unit selection included mappability, relevance for exploration geology and the existence of diagnostic lithological
and/or biostratigraphical criteria for their recognition.
With the available data and time, the construction of
a specific, local sequence framework fell outside the
scope of the working group. Instead, the group tied the
recognised transgressive and regressive events to the
best-fitting sequences in the cycle chart published by
Haq et al. (1988). This Haq et al. (1988) time-scale has
been recalibrated numerically to the scale of Harland
et al. (1990), which was chosen as the current standard
for Dutch stratigraphy. For the sake of completeness,
Figures 4 and 5 (facing pages 226 and 227, respectively)
indicate the Haq et al. (1988) sequence subdivision for
the whole of the Jurassic; Figure 5 provides an overview
of some significant biostratigraphic marker horizons
that were used for calibration of Dutch lithostratigraphy
with the cycle chart. Sequence stratigraphic analysis
was carried out using concepts defined by the Exxon
school, viz. sequences are stratal units bounded by
unconformities and their correlative conformities (Van
Wagoner et al. 1988). In contrast, concepts of genetic
sequence stratigraphy (sensu Galloway 1989), in which
genetic sequences are bounded by maximum flooding
surfaces, are commonly invoked for regional correlation studies. An example of this approach is found in
Partington et al. (1993), for their regional correlation of
the Jurassic of the North Sea area. It should be noted
that their interpretation of Dutch Jurassic sediments was
based on obsolete ideas derived from NAM & RGD
(1980). Figure 4 presents the most modern ideas on the
Dutch chrono-lithostratigraphic development in the
context of the development in the surrounding countries.
Depositional history
The Jurassic succession of the Netherlands can be subdivided into three depositional megasequences. Megasequence I (Rhaetian–Aalenian) reflects the period
between the early and the mid-Cimmerian tectonic
phases. Megasequence II (Aalenian – Middle Callovian)
covers the period of activity of the mid-Cimmerian
phase. Megasequence III (Middle Callovian – Ryazanian)
corresponds to the period between the mid-Cimmerian
and the late Cimmerian (pulse II) phases (RGD 1991a).
Rhaetian–Aalenian (Megasequence I)
This period was characterised by the deposition of a
very uniform blanket of marine shales across large parts
of Northwest Europe. In the Netherlands, these deposits
221
are placed in the Altena Group. After a long period of
restricted marine to continental deposition in the Triassic,
the last pulse of the early Cimmerian extensional phase
in the earliest Rhaetian caused a marine transgression
across large parts of Europe. Very fine-grained deposits
of Rhaetian age, containing abundant lacustrine and
marine fossils, are placed in the Sleen Formation.
Hettangian–Pliensbachian or lowermost Toarcian sediments, consisting of a uniform succession of dark grey
or black silty claystones with abundant pyritised fossil
remains, are called the Aalburg Formation. Towards
the London–Brabant Massif (the southern basin fringe
during the Early Jurassic), an increasing number of thin
limestone beds are intercalated in this unit.
Basin circulation became restricted during the
Toarcian, with anoxic bottom waters and deposition of
a bituminous shaly claystone, called the Posidonia
Formation, over large parts of Northwest Europe. It
constitutes the most prominent oil source rock in the
Netherlands. Basin circulation returned to normal during the Late Toarcian – Bajocian, as indicated by the
deposition of the Werkendam Formation, consisting of
marine silty mudstones and greensands.
Aalenian – Middle Callovian (Megasequence II)
This was a period of significant tectonic activity, which
caused important structural differentiation (Figs 2, 3).
The main effect of the tectonic phase traditionally
addressed in the Netherlands as ‘mid-Cimmerian’ was
the uplift of the Central North Sea dome. The deformation front gradually shifted southwards with time,
resulting in a considerable delay between the timing of
deformation of the dome crest in the Central North Sea
(mid-Aalenian) and the southernmost Dutch provinces
(Kimmeridgian). The amount of intra-Jurassic truncation
decreases away from the dome (Underhill & Partington
1993), and consequently is most severe within the area
of this study in the Dutch Central Graben, the northernmost province of the Netherlands, where open marine
deposition of the Altena Group ceased in the Bajocian.
The Dutch part of the Central Graben remained nondepositional during the Bathonian – Early Callovian. In
the Middle Callovian, deposition gradually resumed, in
a continental facies. The uplift event probably also
affected the Terschelling Basin, the Dutch Lower Saxony
Basin and the Central Netherlands Basin. However, the
evidence for the impact of this phase was removed by
later, more severe truncation in the Jurassic successions
of these basins.
222
The impact of the mid-Aalenian Central North Sea
uplift is negligible in the southern basins (Broad
Fourteens Basin, West Netherlands Basin, Roer Valley
Graben). Werkendam Formation deposition continued,
with an important Bajocian influx of marine sandstones
along the southern basin margin. Depositional facies
changed to shallow marine, sandy carbonates and marls
during the Bathonian (Brabant Formation, ‘Cornbrash
facies’). At least three carbonate–marl cycles were
deposited in the Bathonian to Oxfordian, which are at
present only preserved as erosional remnants in the
southern basins.
In the Dutch Achterhoek (eastern onshore), on the
south-western fringe of the Lower Saxony Basin, a special development is found (Herngreen et al. 1984). The
sedimentary succession up to the Middle Bathonian
shows strong parallels with successions of the Roer
Valley Graben and the German Lower Saxony Basin
proper (Fig. 1). The whole area appears to have been
a single depositional province during this period. At the
transition to the Late Bathonian, however, a differentiation occurred. During the Late Bathonian – Callovian,
an open marine claystone facies was deposited in
Germany and the Achterhoek (informally termed the
Klomps member, Fig. 4). In contrast, deposition of shallow marine sandy carbonates and marls in the Roer
Valley Graben and the West Netherlands Basin persisted into the Oxfordian.
Middle Callovian – Ryazanian
(Megasequence III)
Upper Jurassic – Lower Cretaceous deposits in Northwest
Europe demonstrate a step-by-step overall transgression
from north to south. Periods of marine transgression alternated with phases of short-term progradation of, partly
tectonically controlled, continental siliciclastics. The
continuous shifting of marine and terrestrial realms in
response to syndepositional tectonism and sea-level
fluctuations is reflected by the recurrent intertonguing
of marine and continental sediments. The predominantly marine Scruff Group (Upper Jurassic – Ryazanian)
and Rijnland Group (Lower Cretaceous) interfinger with
the mainly continental Schieland Group (Upper Jurassic
– Barremian) and the paralic to restricted marine
Niedersachsen Group (Upper Jurassic – Ryazanian).
Differential movement of fault blocks was caused by a
combination of oblique-slip effects in an overall extensional regime and halokinesis in areas with salts in the
subsurface (Wong et al. 1989). Together with a high sed-
iment input, this resulted in complex sediment distribution patterns and continuously shifting depocentres.
The cyclic alternation of marine and continental sediments indicates that sediment deposition was also
strongly controlled by sea-level changes.
Middle Callovian – Oxfordian (Stage IIIa)
In the Middle–Late Callovian, predominantly continental sedimentation (Schieland Group) resumed along the
axis of the northern Dutch Central Graben (Fig. 4). The
basal alluvial plain deposits are referred to the Lower
Graben Formation. This unit displays huge thickness variations due to onlap onto syndepositional topography,
and due to differential subsidence. The depositional
area gradually extended into the southern Dutch Central
Graben in the course of the latest Callovian, Oxfordian
and Kimmeridgian. Deposition in the latest Callovian
started with the marginal marine Rifgronden Member
of the Friese Front Formation. It indicates connections
to open marine areas in the northern Central Graben
(Central North Sea), or possible links with the marine
realm in the southern and central Dutch basins.
The shift to deposition of the Middle Graben
Formation in the latest Callovian – Early Oxfordian
reflects an abrupt change to more fine-grained, lakeand swamp-dominated sedimentation. This shift was
accompanied by a short-lived, marine incursion into
the whole Dutch Central Graben, which is correlated
with the maximum flooding surface of sequence LZA4.1 of Haq et al. (1988). During the Middle Oxfordian,
lacustrine conditions prevailed throughout the Dutch
Central Graben. Marine incursions were scarce and
restricted to the far north during the rest of the Oxfordian.
The Oxfordian was a period of significant transgression and onlap. Areas adjacent to the northern
Dutch Central Graben, such as the southern Dutch
Central Graben, Terschelling Basin and Step Graben
were incorporated into the depositional area. Simultaneously, the open marine realm started to expand
southwards into the Dutch Central Graben, first into
block F03 (Middle–Late Oxfordian, sequence LZA-4.2
of Haq et al. 1988). Initially, a stacked prograding
coastal-barrier sand complex (Upper Graben Formation)
developed, behind which a paralic delta plain formed,
represented by the deposits of the Puzzle Hole Formation
(blocks F08–F14). North of the barrier complex, the
Kimmeridge Clay Formation represents the open marine
environment. The coastal sand bodies of the Upper
Graben Formation in the area of block F03 drowned at
the end of the Oxfordian (sequence LZA-4.4 of Haq et
al. 1988). By this time, Kimmeridge Clay deposition
also invaded the Step Graben, onlapping the Upper
Permian Zechstein Group.
Non-marine deposition of the Schieland Group had
already commenced in the Dutch Central Graben during the Callovian, but deposition of the marine Brabant
Formation (Altena Group, Oisterwijk Limestone Member) persisted into the Early–Middle Oxfordian in the
southern Netherlands (Haanstra 1963; NAM & RGD
1980). Cessation of marine Altena Group deposition in
the Roer Valley Graben, the West Netherlands Basin, the
Broad Fourteens Basin and probably the Central
Netherlands Basin – Lower Saxony Basin during the
Late Oxfordian – earliest Kimmeridgian was triggered
by tectonic pulse I of the late Cimmerian. In the Roer
Valley Graben and the West Netherlands Basin, the
Brabant Formation is locally overlain unconformably by
erosional remnants of Late Oxfordian – Portlandian
deposits in continental floodplain facies (Schieland
Group, Nieuwerkerk Formation).
Early–Late Kimmeridgian (Stage IIIb)
During the Kimmeridgian and Portlandian, the northern
Dutch Central Graben became a major depocentre,
accumulating a thick succession of increasingly marine
sediments. The area of deposition once more expanded
significantly. Deposition resumed in continental facies
in the Broad Fourteens Basin, the Dutch Lower Saxony
Basin and the Vlieland Basin (Fig. 4). The depositional
style in the Broad Fourteens and Vlieland Basins
remained continental (floodplain, lacustrine, with occasional sandy fluvial intercalations), with a few marine
incursions. The Vlieland Basin was the site of volcanic
activity in the Middle–Late Jurassic, as the Zuidwal volcanic dome formed (Perrot & van der Poel 1987;
Herngreen et al. 1991). Depending on the time-scale
used, volcanic activity (dated radiometrically at 155–143
Ma) may have taken place somewhere between the
Callovian and the Early Ryazanian.
In the course of the Kimmeridgian, deposition of the
paralic Puzzle Hole Formation in the central Dutch
Central Graben gradually gave way to the open marine
Kimmeridge Clay Formation in the area of blocks
F08–F11. Thin marine sand bodies are found locally in
the uppermost parts of the Puzzle Hole Formation, suggesting the existence of a backstepping coastal-barrier
system. However, much of the character of the transgression cannot be reconstructed due to Subhercynian
223
and/or Laramide erosion (Late Cretaceous – Paleocene).
To the south (blocks F15–F17), the paralic Puzzle Hole
Formation grades into deposits characterised by continental alluvial plain facies (Delfland Formation of
Herngreen & Wong, 1989; now called Friese Front
Formation). In the southern Dutch Central Graben, alluvial plain deposition replaced the predominantly lacustrine deposition around the end of the Oxfordian. During
the Early Kimmeridgian (LZA-4.4 of Haq et al. 1988),
the depositional area in the southern Dutch Central
Graben expanded. Seismic and palaeogeographic information suggest that the boundaries between the areas
of deposition of the Puzzle Hole Formation, the
Kimmeridge Clay Formation and the Friese Front
Formation were determined by faults.
In the Broad Fourteens Basin, widespread deposition commenced in the Early Kimmeridgian (LZA-4.5
of Haq et al. 1988), with the accumulation of sandy
alluvial plain sediments referred to the Aerdenhout
Member of the Breeveertien Formation (Fig. 4). This
member unconformably overlies deposits of the Altena
Group or the Upper Germanic Triassic. The progressive transgression observed in the Central Graben coincides with a shift from alluvial plain (Aerdenhout
Member) to lacustrine and lagoonal deposition
(Fourteens Claystone Member) in the Broad Fourteens
Basin (associated with the maximum flooding surface
of sequence LZA-4.6 of Haq et al. (1988). Deposition
of the Basal Weiteveen Clastic Member in the Dutch
Lower Saxony Basin (= Niedersachsen Basin) seems to
have started close to the end of the Early Kimmeridgian.
The introduction of coarser siliciclastics in the Dutch
Central Graben (main Friese Front member, Puzzle Hole
Formation and Upper Graben Formation), the Broad
Fourteens Basin (Breeveertien Formation, Aerdenhout
Member) and the Dutch Lower Saxony Basin (Weiteveen
Basal Clastics Member) coincided with the start of the
late Cimmerian phase (Haanstra 1963; ’t Hart 1969; ‘Late
Kimmerian I pulse’ of RGD 1991b). The resulting uplift
terminated the first depositional phase of the Nieuwerkerk Formation in the most rapidly subsiding areas of
the Roer Valley Graben and the West Netherlands Basin.
Late Kimmeridgian – earliest Portlandian (Stage IIIc)
In the Late Kimmeridgian, the ongoing transgression led
to the first marine influence on sedimentation in the
southern Dutch Central Graben and the Terschelling
Basin. This is witnessed by the deposition of the marineinfluenced Oyster Ground Member (Friese Front For-
224
mation, Fig. 4). Two distinct transgressive phases are
identified; in the early Late Kimmeridgian, the transgression reached block F18, while block L02 became
transgressed by the latest Kimmeridgian. These events
are tentatively correlated with the transgressive systems
tracts of sequences LZA-4.7 and LZB-1.1 of Haq et al.
(1988). The latter flooding event is associated with
onlap onto exposed Triassic and Permian rocks in the
Terschelling Basin (Oyster Ground Member in block
F15) and the Vlieland Basin – Central Netherlands Basin
area (continental Zurich Formation). At the same time,
tectonic tilting and associated halokinesis caused the
depocentre of the Dutch Central Graben to shift from
the central–eastern axis (from block F03, extending
southwards into blocks L03–F18) to the western graben
margin (block F02–L05). The seismic cross-section of
the graben system shows this westwards shift (Fig. 6).
During the Late Kimmeridgian – Portlandian, siliciclastic deposition in the Lower Saxony Basin was periodically replaced by accumulation of evaporites and
carbonates (evaporitic and marl members of the
Weiteveen Formation, Fig. 4). These cycles may be correlatable with the alternation of coarser clastics and
fines with minor evaporites found in the Broad Fourteens
Basin (Breeveertien Formation, several members). The
lithofacies (carbonates, marls, evaporites, coals) of the
Zurich Formation in the remnants of the Central
Netherlands Basin (‘Voorthuizen subbasin’ of Haanstra
1963; Gouwzee Trough of RGD 1993a) are similar to
those in the Niedersachsen Group in the Dutch Lower
Saxony Basin.
In the West Netherlands Basin and the Roer Valley
Graben, lacustrine and alluvial plain deposition was
restricted to those fault blocks undergoing strongest
subsidence. A progressive depositional onlap is seen
in the Portlandian–Ryazanian section. In each consecutive depositional sequence, higher basin-fringe fault
blocks became part of the depositional area. Very thick
successions of proximal alluvial plain deposits can be
found in places.
In the Portlandian and Ryazanian, deposition resumed
in the Central Netherlands Basin. The depositional style
is transitional between the mainly lacustrine and evaporitic facies of the Lower Saxony Basin and the paralic
and restricted marine facies of the Central Graben – Vlieland Basin. Deposition in the southern province (West
Netherlands Basin and the western Roer Valley Graben)
ceased due to uplift in the Kimmeridgian (around the
lower sequence boundary of LZB-1.1 of Haq et al. 1988).
Non-deposition lasted until the latest Portlandian –
Ryazanian. From then on, continental sediments were
deposited; marine conditions did not reach this area until
the Late Hauterivian – Barremian.
Portlandian (Stage IIId)
During the Early Portlandian, the ongoing transgression resulted in deposition of the Terschelling Member
of the Friese Front Formation, reflecting coastal deposition along the southern fringe of the Dutch Central
Graben (blocks L09–L12, sequences LZB-1.2, -1.3 of
Haq et al. 1988). To the north, the Friese Front Formation
grades into the open marine Scruff Greensand Formation
in the southern Dutch Central Graben. Thick, sand-dominated successions of Portlandian–Ryazanian age were
deposited here (blocks F15–F18, sequences LZB-1.3 to
-1.5 of Haq et al. 1988). Equivalent, thinner sand tongues
are found in the eastern Terschelling Basin, the Vlieland
Basin and the northern Dutch Central Graben (blocks
F03–F05). During this period, the Vlieland Basin became
divided into two subbasins, separated by the Zuidwal
volcanic dome (Herngreen et al. 1991). During the Early
Portlandian, marine conditions only prevailed in the
northern subbasin. The southern subbasin was characterised by continental (lacustrine to lagoonal) deposition.
The Scruff Greensand Formation grades into the
Kimmeridge Clay Formation in the northern Dutch
Central Graben. The depocentre of the open marine
Kimmeridge Clay Formation, which prior to the
Portlandian was situated in this northern area, abruptly
shifted to the southernmost Central Graben and the
northern Vlieland Basin. In the southern B-quadrant,
basin circulation stagnated during the Portlandian. This
resulted in deposition of the bituminous claystones of
the Clay Deep Member. Euxinic marine conditions
became more widespread in the northern Dutch Central
Graben during the Ryazanian (sequence LZB-1.5 and
particularly LZB-1.6 of Haq et al. 1988).
Late Portlandian – Ryazanian (Stage IIIe)
During the Late Portlandian (sequence LZB-1.5 of Haq
et al. 1988), marine conditions (Scruff Greensand Formation) briefly reached the entire Vlieland Basin. In
the southern Dutch Central Graben, the marine basin
became shallower, inducing the northwards progradation of shallow marine, spiculitic greensands (Scruff
Spiculite Member). Even the more elevated areas (for
example over salt domes) of the Dutch Lower Saxony
Basin and Central Netherlands Basin, which had thus
far remained exposed, became inundated by the sea.
In the latter basin, the depositional area expanded to
the north-west.
In the Broad Fourteens Basin, this overall regressive
tendency is reflected by the transition within the
Breeveertien Formation from lacustrine and lagoonal
coastal plain fines (Fourteens Claystone Member and
Driehuis Mottled Claystone Member) to widespread
sandy alluvial plain deposits (Bloemendaal Member).
In the Dutch Lower Saxony Basin, the Late Portlandian
shoaling trend is demonstrated by the Serpulite Member
of the Weiteveen Formation. This widespread carbonate deposit marks the culmination of clastic starvation
in this area.
Deposition of evaporites and carbonates with subordinate siliciclastics (Weiteveen Formation) in the Lower
Saxony Basin was replaced by open water lacustrine
deposition (Coevorden Formation) at the beginning of
the Ryazanian. This event is interpreted as indicative
of a flooding phase that correlated with the transition
from the sandy fluvial Bloemendaal Member to the
lagoonal Neomiodon Claystone Member (both of the
Breeveertien Formation) in the Broad Fourteens Basin.
This period was also marked by widespread deposition
of sediments referred to the Nieuwerkerk Formation in
the Roer Valley Graben and West Netherlands Basin;
thick successions of locally coarse alluvial plain sediments were deposited on rapidly subsiding fault blocks
along the axes of the basins. The depositional area continued to expand gradually. The basin margins were
either covered by a thin, condensed succession (e.g.
locally in the province of Groningen), or remained
exposed and non-depositional.
Late Ryazanian (Stage IIIf)
During the Ryazanian (sequence LZB-1.6 of Haq et al.
1988), the stagnant marine basin area in the northern
Dutch Central Graben expanded southwards into block
F05. Deposition of the Clay Deep Member completely
superseded Scruff Greensand Formation deposition
around the mid-Ryazanian. This change in depositional
style coincided with the first signs of tectonic pulse II
of the late Cimmerian (RGD 1991a). This also caused
local truncation of the Scruff Greensand Formation and
the Friese Front Formation in the southern Central
Graben (parts of blocks L02–05). Initially, sedimentation of the Scruff Greensand Formation resumed briefly
(Stortemelk Member, correlated with the lowstand of
225
sequence LZB-1.6 of Haq et al. 1988). Subsequently, the
deep marine basin expanded markedly southwards,
depositing Kimmeridge Clay Formation sediments (Schill
Grund Member) in the previously shallow marine to continental realm. This marine incursion also reached the
Vlieland Basin, where the Stortemelk Member is found
intercalated with lagoonal–lacustrine deposits of the
Zurich Formation. In the Broad Fourteens Basin, tectonic pulse II of the late Cimmerian is expressed as two
minor unconformities (base and intra-Neomiodon
Claystone Member, Breeveertien Formation).
In the Dutch Central Graben, large-scale differential subsidence ended with tectonic pulse II of the late
Cimmerian (mid-Ryazanian and earliest Valanginian).
From then on (sequence LZB-2.1 of Haq et al. 1988),
a more uniform sedimentation pattern started, associated with the post-rift thermal sag phase. This is illustrated by the contrast between the highly variable
thickness of the succession underlying the Stortemelk
Member and the more uniform development of the
post-uplift succession (Clay Deep Member, Stortemelk
Member and Schill Grund Member). In the Broad
Fourteens Basin, the West Netherlands Basin and the
Roer Valley Graben, the highly differential subsidence
patterns continued at least throughout the Valanginian.
Subsequent history
The expansion of the marine sedimentation area continued during the Cretaceous, until eventually the
London–Brabant Massif became flooded in the
Campanian–Maastrichtian. The Jurassic successions in
the Dutch subsurface were deformed by several later
tectonic phases. The Santonian–Campanian (Subhercynian) and Early Paleogene (Laramide) inversion phases
had the most severe impact. During these compressive
events, the Jurassic depocentres were inverted (van
Wijhe 1987). Practically all Jurassic sediments were
removed along the inversion axes of these basins. At
present, the occurrences of Jurassic rocks are restricted
to the basinal areas (Fig. 3). Subsequent Tertiary subsidence in the Netherlands was more or less evenly
distributed. Subsidence rates were highest in the northern Dutch offshore, however, and Tertiary (particularly Neogene) sediment distribution patterns are dominated by large-scale progradation in this direction.
226
Petroleum geology
Several Jurassic formations have economic significance
in the Netherlands, either as reservoirs or as oil source
rocks. Figures 1 and 4 show the stratigraphic positions
of the units mentioned in this context below, and their
equivalents in neighbouring countries. The Toarcian
Posidonia Formation is the most prominent oil and wet
gas source rock in the Dutch subsurface (Bodenhausen
& Ott 1981), to which the majority of the oil reserves
in the country can be attributed. Additional oil sourcing potential can be attributed to certain lacustrine strata
of the Coevorden Formation (Ryazanian) in the Lower
Saxony Basin. This interval is also known to act as an
oil source rock in adjacent parts of Germany. The highly
bituminous Clay Deep Member (Ryazanian) of the
Kimmeridge Clay Formation in the northern sector of
the Dutch Central Graben has oil-sourcing potential.
However, the areal distribution and stratigraphic range
of this deposit is much smaller than that of equivalent
bituminous intervals in the Kimmeridge Clay Formation
(and equivalents) in the UK, Danish and Norwegian offshore, where it constitutes one of the major oil source
rocks.
Coal occurrences in the Lower Graben Formation
(Middle–Upper Callovian), the Middle Graben Formation
(Oxfordian), the Puzzle Hole Formation (mainly
Kimmeridgian) and the Friese Front Formation (uppermost Callovian – Portlandian) may locally have sourced
wet gas. However, in most areas, burial was insufficient to reach the gas window (Wong et al. 1989). On
the other hand, gas source rocks of Late Carboniferous
age are more or less ubiquitous throughout the
Netherlands. The main problem for gas generated from
these older rocks is to pass through the cover of Permian
salts and reach the Jurassic. Furthermore, the maximum
burial depths of the Carboniferous strata, for instance
in the Central Graben, may have caused these rocks to
become overmature.
At present, oil and gas reserves have been discovered in the Lower Graben Formation (Middle–Upper
Callovian), Upper Graben Formation (uppermost
Oxfordian), Scruff Greensand Formation (Portlandian)
and Friese Front Formation (uppermost Callovian –
Portlandian) in the Central Graben area. Some sandstone
members of the Breeveertien Formation (Kimmeridgian–
Ryazanian) in the Broad Fourteens Basin were found
to be oil-bearing. In the West Netherlands Basin, the
Ryazanian and younger levels of the Nieuwerkerk
Formation are prospective. The Middle Werkendam
Member (Bajocian) and carbonate members of the
227
TWT sec
3.0
2.0
1.0
Upper Germanic Trias Gp
Lower Germanic Trias Gp
Scruff Greensand Fm.
Chalk Gp
Rijnland Gp
Clay Deep Mb.
Lower North Sea Gp
F11-03
Kimmeridge Clay Fm
Altena Gp
Posidonia Shale Fm
Lower Graben Fm
Middle Graben Fm
Zechstein
Salt Fm
F09-01
Puzzle Hole Fm
ENE
ENE
Euxinic restricted marine claystones (Clay Deep Mb (Kimmeridge Clay Fm), Posidonia Shale Fm)
Open marine claystone (Vlieland Claystone Formation)
Open marine & lagoonal claystone (Kimmeridge Clay Formation, Altena Group)
Open marine argillaceous sandstone/greensand (Scruff Greensand Formation)
Shallow marine/coastal sandstone (Upper Graben Formation)
Coal-rich coastal plain (Puzzle Hole Formation)
Fine-grained fluvial plain, overbank dominated (Middle Graben Formation)
Sandy fluvial plain, channel dominated (Lower Graben Formation)
Depositional setting/seismic facies
Intra-Triassic level II (Muschelkalk Evaporite Member)
Intra-Triassic level III (near-base Middle Buntsandstein Subgroup)
Base Lower Germanic Trias Group (base Lower Buntsandstein Formation)
Puzzle Hole Fm.
Upper Graben Fm
F08-02
Fig. 6. Seismic cross-section, running WSW–ENE across the Dutch sector of the Central Graben (Fig. 2). The Jurassic – Lower Cretaceous section has been colour-coded according
to the main depositional facies.
Base North Sea Groups
Base Chalk Group
Base Valanginian
Base Puzzle Hole Formation, Friese Front Formation
Base Scruff Greensand Formation
Base Kimmeridge Clay Formation; Oyster Ground Mb
Base Upper Graben Formation
Base Middle Graben Formation
Base Lower Graben Formation
Base/top Posidonia Shale Formation
Base Altena Group (base Sleen Formation)
Intra-Triassic level I (near-base Keuper Formation)
Reflectors
Zechstein
Salt Fm
WSW
Brabant Formation (Callovian–Oxfordian) have locally
been shown to be oil-bearing in the Roer Valley Graben
and the West Netherlands Basin.
Exploration of the Jurassic in the Netherlands has
reached a mature stage. The acquisition of high-quality seismic and well data and the good biostratigraphic
control obtained in recent years have resulted in a clear
regional geological picture. These data also allow, for
the first time, the application of sequence stratigraphy.
Integration of sequence stratigraphic concepts into the
revision of Dutch lithostratigraphy (van Adrichem
Boogaert & Kouwe 1994–1997) has resulted, in particular, in a far better understanding of the Upper Jurassic
stratigraphy of the Netherlands.
Acknowledgements
The authors wish to thank the Geological Survey of the
Netherlands (Rijks Geologische Dienst – RGD/NITG) for
permission to publish the presented data. The authors
are indebted to R. Rijkers, A. Hollen and F. Rispens (all
RGD) for providing information on the regional distribution and petroleum exploration successes in the
Dutch Jurassic. H.A. van Adrichem Boogaert and M.C.
Geluk (RGD) gave valuable comments to the manuscript
and its precursors. Similarly, the manuscript has benefited significantly from earlier discussions with the various members of the working group on the Upper
Jurassic – Lower Cretaceous Stratigraphy for the new
Stratigraphic Nomenclature of the Netherlands.
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229
ε7
ε6
Bathonian
161.3
4.5
4.4
ε1-4
2.2
GSP
Kim.
Clay
Fm
CFT
GSA
ATBR1
Scruff Greensand
Fm
Open marine argillaceous greensand
Shallow marine greensand
GSB
CFO
Brabant
Fm
Puzzle Hole Fm U. Graben Fm
M. Graben Fm
L. Graben Fm
Lagoonal claystones/siltstones
Lacustrine/highly restricted marine carbonates
CMS
Upper Werkendam
Claystone Mb
4.4
UAB-4
Toarcian
Lower Werkendam
Claystone Mb
4.5
ζ
ε2
Middle Werkendam Mb
1.1
4.6
4.3
ε1
187.0
β2
β1
Werkendam Fm
?
209.5
Hettangian
208.0
Rhaetian
Norian
Abbreviated stratigraphic terms
ATBRO:
ATBRU:
ATBR3:
ATBRM:
ATBR2:
ATBRL:
ATBR1:
Oisterwijk Limestone Mb
Upper Brabant Marl Mb
Upper Brabant Limestone Mb
Middle Brabant Marl Mb
Middle Brabant Limestone Mb
Lower Brabant Marl Mb
Lower Brabant Limestone Mb
Middle Graben Sandstone Mb
Friese Front Formation
Posidonia
Shale Fm
CFO:
CFT:
CFR:
Oyster Ground Claystone Mb
Terschelling Sandstone Mb
Rifgronden Claystone Mb
Weiteveen Formation
F:
E:
D:
C:
B:
A:
3.4
3.3
3.2
3.1
203.5
α2
α1
Shallow marine sandy limestone
CMS:
Aalburg Fm
α3
Highly restricted marine anhydrite/carbonates
Middle Graben Formation
4.1
γ1
β3
Highly restricted marine salts
4.2
δ1
γ3
γ2
UAB-3
Lias
δ2
Sandy coastal/fluvial plain heterolithics
Brabant Formation
Altena Group
LZA-1
Aalenian
β1
α
Coal-rich coastal plain heterolithics
Fine-grained coastal plain and lacustrine heterolithics
δ1
β2-4
Coastal sand
Kimmeridge
Clay Fm
?
?
ATBRL
Bituminous marine clay/shale
Clay Deep Mb
Scruff Group
Niedersachsen Gp
Schieland Group
Schill Grund Mb
Friese Front Fm
Klomps mb
ATBR2
3.1
LZA-2
Dogger
Bajocian
A
KN
GSS
CFR
ATBRM
2.1
178.0
Pliensbachian
Breeveertien Fm
Fourteens Claystone Mb
3.2
ε5
F
E
D
C
B
ATBRU
γ
Sinemurian
Weiteveen Fm
Zurich Fm
ATBR3
2.4
173.5
194.5
Driehuis Mb
Santpoort
Mb
Marl
Open marine clay (Jurassic)
Coevorden Fm
ATBRO
4.3
2.3
δ2
Bloemendaal Mb
Depositional facies
Open marine clay (Cretaceous)
Aerdenhout Mb
4.2
4.1
LZA-3
ζ
Nieuwerkerk
Fm
Dutch Central Graben
KN
Neomiodon Mb
Nieuwerkerk
Fm
N
Schieland
β
α
4.6
Lower Saxony
Basin
KN
Schieland Group
4.7
Central Netherlands
Basin Achterhoek
Schieland Gp
Sequences
after Haq et al.
(1988)
LZB-1
Tethys
Boreal
γ−ζ
157.1
166.1
1.4
1.1
Callov.
West Netherlands Broad Fourteens
Basin
Basin
1.5
1.3
Oxford.
Roer Valley
Graben
1.6
1.2
154.7
S
LZB-2.1
LZA-4
Kimmeridgian
152.1
Kim.
147.8
Tithonian
145.6
Malm
142.8
Valang.
Berrias.
140.7
Global
after
Harland
et al.
(1990)
Substages
Stratigraphy
Portlandian Ryaz.
Time
(Ma)
UAB-2
UAB-1
UAA-4
RN
Sleen Fm
Fig. 4. Litho-chronostratigraphic scheme of the Rhaetian–Ryazanian succession of the five main Jurassic basin systems in the Netherlands: (1) Roer Valley Graben – West Netherlands Basin, (2) Off-Holland Low – Broad Fourteens Basin, (3) Central
Netherlands Basin, (4) Ems Low – Lower Saxony Basin and (5) Vlieland Basin, Terschelling Basin and Dutch Central Graben. Abbreviated stage names are given in full in Fig. 1; Berrias., Berriasian. Compiled and modified from van Adrichem
Boogaert & Kouwe (1994–1997, sections F, G).
Serpulite Mb
Upper Marl Mb
Upper Evaporite Mb
Lower Marl Mb
Lower Evaporite Mb
Basal Clastic Mb
Scruff Greensand Formation
GSS:
GSP:
GSA:
GSB:
Stortemelk Mb
Scruff Spiculite Mb
Scruff Argillaceous Mb
Scruff Basal Sandstone Mb
KN:
RN:
Rijnland Gp
Upper Germanic Trias Gp
Stratigraphy
Bejuia polygonalis
Meiourogonyaulax valensii
tenuiplicatus
zigzag
Kraeuselisporites
tubbergensis
top acme
base acme
macer
suessi
marshi
planorbis
liasicus
angulata
bucklandi
(f) foraminifer
(o) ostracod
r rare
Rhaetogonyaulax spp.
Dapcodinium priscum
Liasidium variabile
c consistent
semicostatum
turneri
obtusum
oxynotum
raricostatum
jamesoni
ibex
davoei
margaritatus
spinatum
tenuicostatum
sporomorph appearances and
disappearances are approximate
Cingulizonates rhaeticus; Cornutisporites seebergensis;
Densosporites fissus; Lunatisporites rhaeticus;
Rhaetipollis germanicus; Semiretisporis spp.;
Triancoraesporites reticulatus;
Tsugaepollenites pseudomassulae; Zebrasporites laevigatus
Ovalipollis pseudoalatus
Cerebropollenites spp.
Ricciisporites tuberculatus; Zebrasporites interscriptus
Contignisporites problematicus
c Heliosporites altmarkensis
Leptolepidites spp.; Sestrosporites pseudoalveolatus
Calliasporites spp.; Neoraistrickia truncata
Rhombocythere penarthensis (o)
Cytherelloidea buisensis (o); Lingulina tenera collenoti (f);
Lutkevichinella sp. (o)
Ogmoconchella ellipsoidea (o); Cytherelloidea circumscripta (o);
Cytherelloidea pulchella (o); Klinglerella translucens (o)
Ogmoconcha hagenowi (o); Nanacythere elegans (o)
Lophodentina pumicosa (o); Ektyphocythere betzi (o);
Ektyphocythere triebeli (o); Lophodentina lacunosa (o)
Klinglerella variabilis (o)
Pleurifera harpa (o); Gammacythere ubiquita (o);
Ogmoconchella bispinosa (o); Gramannicythere bachi (o);
Ogmoconcha amalthei (o); Bairdia clio (o); Polycope cincinnata (o)
Wicherella semiora semiora (o); Gramannella apostolescui (o)
Ogmoconcha contractula (o); Trachycythere tubulosa (o);
Saracenaria sublaevis (f); Bolivina liasica liasica (f)
Frondicularia terquemi (f)
Lingulina tenera group (f); Marginulina prima group (f)
Otocythere callosa (o); Aphelocythere kuhni (o);
Camptocythere praecox (o); Lenticulina foveolata (f)
Camptocythere foveolata (o)
Camptocythere media (o)
serpentinus
Ischyosporites variegatus; Staplinisporites
(incl. Coronatisporites)
c Rogalskaisporites cicatricosus
Trilites spp.
Neoraistrickia gristhorpensis; Uvaesporites
argenteaeformis; c Densoisporites;
Sestrosporites pseudoalveolatus
Circulina meyeriana
Chasmatosporites major
Kinkelinella persica (o)
Luehndea spinosa
Parvocysta spp.; Reutlingia spp.;
Susadinium spp.; c Phallocysta eumekes
Scriniocassis weberi
Praeschuleridea decorata (o); Camptocythere pusilla (o)
Glyptocythere polita (o)
bifrons
variabilis
thouarsense
dispansum
pseudoradiosa
aalensis
opalinum
murchisonae
bradfordensis
concavum
discites
laeviuscula
propinquans
Glyptocythere scitula (o); Fuhrbergiella horrida horrida (o);
Ljubimovella piriformis (o)
humphriesianum
Ammopalmula infrajurensis (f); Fuhrbergiella gigantea (o);
Pleurocythere impar (o); Glyptocythere tuberodentina (o)
Pleurocythere richteri (o)
Pleurocythere regularis (o)
Glyptocythere auricula (o)
Progonocythere stilla (o); Glyptocythere guembeliana (o)
Micropneumatocythere subconcentrica (o);
Oligocythereis fullonica (o)
Progonocythere polonica (o); Lophocythere plena (o)
Pleurocythere connexa (o); Lenticulina quenstedti (f)
Lophocythere interrupta interrupta (o)
Lophocythere scabra scabra (o); L. bipartita (o);
Pseudohutsonia tuberosa (o)
Vernoniella sequana (o)
Lophocythere multicostata (o)
Nophrecythere cruciata oxfordiana (o)
Pseudoperissocytheridea parahieroglyphica (o);
Eucytherura costaeirregularis (o)
Eucytherura horrida (o)
Lophocythere flexicosta (o); Nophrecythere cruciata cruciata (o);
Epistomina mosquensis (f)
Mandelstamia rectilinea (o)
Schuleridea triebeli (o); Galliaecytheridea wolburgi (o)
Galliaecytheridea punctata (o); Macrodentina cicatricosa (o);
Eripleura eleanorae (o); Galliaecytheridea dissimilis (o)
Mandelstamia maculata (o); Epistomina nuda (f)
Eocytheridea eusarca (o); Galliaecytheridea volgaensis (o);
Macrodentina rugulata (o); Macrodentina transiens (o);
Exophthalmocythere gigantea (o); Klieana calyptroides (o)
Paranotacythere elongatata (o); Galliaecytheridea compressa (o)
Galliaecytheridea polita (o); Paralesleya perforata (o)
Galliaecytheridea spinosa (o); Mandelstamia tumida (o);
Saracenaria oxfordiana (f); Aaleniella inornata (o)
Fabanella ansata (o); Mantelliana purbeckensis (o)
Cypridea carinata (o); C. granulosa (o)
Galliaecytheridea postsinuata (o); Klieana dictyota (o)
Mandelstamia sexti (o); Cytheropterina triebeli (o);
Galliaecytheridea teres (o); Paranotacythere speetonensis (o);
Schuleridea juddi (o)
Ammovertella cellensis (f); Protocythere hannoverana (o);
Protocythere pseudopropria (o)
Selected foraminifer/ostracod datums
Fuerbergiella primitiva (o)
Calliasporites segmentatus
Precicatricosisporites spp.
Calliasporites segmentatus; Lycopodiacidites rugulatus;
Neoraistrickia truncata; Uvaesporites argenteaeformis;
c Lycopodiumsporites semimuris
Raistrickisporites brevitruncatus
Precicatricosisporites
c Concavissimisporites; c Impardecispora;
c Trilobosporites; Kraeuselisporites sp.
Classopollis echinatus/hammenii plexus
c Cicatricosisporites
Classopollis
Parvisaccites radiatus
Classopollis
Aequitriradites; Plicatella
Clavifera triplex
various Trilobosporites spp.
Selected sporomorph datums
niortense
garantiana
Nannoceratopsis dictyambonis; N. triceras;
Wallodinium cylindricum
Carpathodinium predae
parkinsoni
c R. aemula;
Wanaea
Ctenidodinium combazii/ornatum plexus
Rhynchodiniopsis regalis; Valvaeodinium spinosum
Nannoceratopsis spiculata; N. gracilis
L. scarburghensis
L. scarburghensis
C. continuum
Lithodinia jurassica;
c Pareodinia prolongata
N. pellucida; S. crystallinum
E. luridum
c P. pannosum
Stephanelytron; S. fasc./penic.
P. pannosum
A. dictyota; P. pannosum
r G. jurassica; r O. patulum
O. patulum
S. inritibilum
c Cribroperidinium sp. A/B; E. polyplacophorum
C. panneum; G. dimorphum
G. mutabilis;
S. jurassica
c Muderongia sp. A
G. virgula
T. daveyi
D. spinosum; E. torynum; K. porosispinum
Gonyaulacysta sp. A; R. thula
B. radiculatum
E. pharo
c P. ‘eopelliferum’ sensu RRI (1987)
T. apatela
M. extensiva
Selected dinoflagellate datums
morrisi
subcontractus
progracilis
calloviense
macrocephalus
discus
orbis
hodsoni
jason
coronatum
base occurrence
UAA-4
UAB-1
2.1
3.1
3.2
3.3
3.4
4.1
4.2
4.3
4.4
4.5
4.6
1.1
2.1
2.2
2.3
2.4
3.1
3.2
lamberti
athleta
autissiodorensis
eudoxus
mutabilis
cymodoce
baylei
rosenkrantzi/regulare
serratum/glosense
tenuiserratum
densiplicatum
cordatum/mariae
elegans
hudlestoni
wheatleyensis
scitulus
pectinatus
‘oppressus’/anguiformis
kerberus
okusensis
glaucolithus
albani
fittoni
rotunda
pallasioides
primitivus
preplicomphalus
lamplughi
albidum
stenomphalus
icenii
runctoni
kochi
Paratollia
Polyptychites
Dichotomites
unnamed
top occurrence
Norian
Rhaetian
α1
α2
α3
β1
β2
β3
γ1
γ2
γ3
δ1
δ2
ε1
ε2
ζ
α
β1
β 2–4
γ
δ1
δ
2
ε 1–4
ε
ζ
4.1
4.3
4.2
4.4
4.5
4.6
4.7
1.1
1.2
1.3
1.4
1.5
1.6
2.1
2.2
2.3
NW European
Standard Ammonite
Zonation
Fig. 5. A selection of diagnostic biomarker horizons for the Rhaetian–Valanginian, correlated with the Northwest European standard ammonite zonation. The Haq et al. (1988) cycle chart
has been recalibrated to fit the time-scale of Harland et al. (1989). Kimmeridgian s.l. equals Kimmeridgian sensu anglico. The terms Lias, Dogger and Malm and their classic regional subdivisions as depicted in the various figures are used in order to show the stratigraphic position of the sediments found in the Netherlands in a European context of well-established zonations. Compiled and modified from van Adrichem Boogaert & Kouwe (1994–1997, sections F, G).
210
205
200
195
190
185
180
175
170
165
160
155
150
145
140
135
Time
(Ma)
Cretaceous
Late Jurassic
Middle Jurassic
Early Jurassic
Triassic
L
E
L
E
‘L’
Valanginian
Berriasian
Tithonian
Kimm.
Oxfordian
Ryazanian
Portlandian
Kimmeridgian s.l.
‘E’
L
E
L
M
E
L
M
E
L
Callovian
Bathonian
Bajocian
Aalenian
Toarcian
Pliensbachian
Sinemurian
Hettangian
Malm
Dogger
Lias
M
E
L
E
L
E
Sequences
(Haq et al.
1988)
LZB-2
LZB-1
LZA-4
LZA-3
LZA-2
LZA-1
UAB-4
UAB-3
UAB-2