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Terug naar StartpaginaONDERGRONDMODELLEN TOELICHTING NOMENCLATOR

Nomenclator Ondiep

Nomenclature (Deep)

Table

Overview

Tertiary and Quaternary

Upper Cretaceous

Upper Jurassic and Lower

Cretaceous

Rijnland Group KN

Niedersachsen Group SK

Scruff Group SG

Schieland Group SL

References Upper

Jurassic/ Lower

Cretaceous

Middle and Lower Jurassic

Triassic

Permian

Carboniferous

Devonian

Upper Jurassic and Lower CretaceousExisting Late Jurassic stratigraphy was established in 1980 when NAM and RGD published the

‘Stratigraphic Nomenclature of the Netherlands’. Van Adrichem Boogaert and Kouwe revised the

standard in 1993-1997. The lithostratigraphical classification was based on various regional

publications of the Upper Jurassic, e.g. by Brown in Glennie (1990), Cameron et al. (1992),

Frandsen et al. (1987), Herngreen & Wong (1989), Herngreen et al. (1991), Michelson & Wong

(1991) and Ziegler (1990). New data gathered from continued exploration in the Dutch Central

Graben and adjacent Terschelling Basin during the past twenty years (1993-2012) resulted in an

improved understanding of the latest Middle Jurassic to earliest Cretaceous, Callovian-

Ryazanian, siliciclastic successions. Several studies contributed to this progress, e.g.: Abbink et

al. (2006), Herngreen et al. (2000, 2003), Duin et al. (2006), Wong (2007), Andsbjerg & Dybkjaer

(2003), Michelsen et al. (2003), Johannessen (2003), Fraser et al. (2003), Coward et al. (2003)

and Lott et al. (2010). New palynological techniques (e.g. Sporomorph Ecogroups in Abbink,

1998) and newly acquired sedimentological, lithological, stratigraphic and seismic data led to the

identification of three well recognizable unconformities or their correlatable conformities in the

late Middle Jurassic to earliest Cretaceous. These (un-)conformities resulted in the definition of

three major stratigraphic sequences in the Late Jurassic and one in the overlying earliest

Cretaceous interval. The unconformities and stratigraphic units in-between are related to to

tectonic, climatic, environmental and stratigraphic even ts (Abbink et al., 2006). The recognition of

these sequences in wells in the Central Graben and Terschelling Basin showed the present

lithostratigraphic scheme to be outdated for consistent stratigraphic in terpretation. Hence the

necessity arose to revise and update the Late Jurassic succession of the Stratigraphic

Nomenclature for the subsurface of the northern Dutch offshore area. In order to reach broad

acceptance and a general consensus, cooperation was sought and obtained from the E&P

industry and consultants. A series of workshops and (inter)national presentations were organized

on this topic from 2010-2012. The recommendations from these meetings and discussions

afterwards are integrated in the present contribution (see pdf ).

For a good understanding of the studied interval and correct application of the presented

lithostratigraphy, detailed information is incorporated in the definitions. All definitions include

detailed descriptions of lithology, boundaries, depositional setting, sequence stratigraphic

interpretations, and ages. Reference is made to diagnostic fossil species, including

dinoflagellates, sporomorphs, foraminifers and ostracods. Presented biostratigraphic data is

derived from RGD/TNO studies and publications, and various company and consultancy reports.

A TNO s electio n o f dia gnostic bioma rker horizo ns, co rrelated with the s tandard ammoni te

zonation for Northwest Europe, is presented in the biomarker Table I (see pdf ). Specific details

regarding the Jurassic-Ryazanian interval, including detailed bioevents, are recorded in

Munsterman et al. (2012) and will be published in Verreussel et al. (in prep.).

Geological historyThe Permian, Triassic and Early Jurassic were periods of relative tectonic quiescence in the

Netherlands (De Jager, 2007). During the Triassic, a rifting phase related to the Mesozoic break-

up of the Pangea supercontinent commenced in the Artic-North Atlantic and between Greenland

and Scandinavia (Lott et al., 2010). During the Jurassic, an eastern branch of the incipient rift

basins/structures protruded into the North Sea area (Ziegler 1988, 1990). As such the structural

outline of the Netherlands progressively changed from a single large basin, the Southern Permian

Basin, into a multi-basinal pattern during the Late Jurassic (Wong, 2007; Fig. 3).

The slow regional subsidence in pre-rift (Early Jurassic) times led to the accumulation of the

predominantly marine argillaceous deposits of the Altena Group. In general, regional extension

was east-west directed. An uplift phase ended the largely uniform subsidence and sheet-like

deposition of Middle Jurassic sediments. This uplift, related to the development of a thermal dome

in the central North Sea area during the Aalenian to Bathonian (Mid-Kimmerian tectonic phase),

caused wide- spread erosion and non-deposition (Underhill & Partington, 1993; Andsbjerg &

Dybkjaer, 2003). It created a hiatus between the Late Jurassic and underlying Middle to Early

Jurassic or older strata in the northern Dutch offshore. In the Middle Callovian, rifting starts in the

Dutch area and continues until the base of the Valanginian. At first, rifting only affected the

relatively narrow area of the graben axis. This phase is referred to as Sequence 1 in Abbink et al.

(2006). During the Late Kimmeridgian, a change in the tectonic regime occurs in the southern

North Sea. Extension direction changes from E-W to SW-NE (Zanella & Coward, 2003). Numerous

old lineaments/ structures were rejuvenated, which resulted in the opening of the Terschelling

Basin and the Step Graben as peripheral basins of the Central Graben and initiates the end of

subsidence in some parts of the Central Graben. This phase coincides with Sequence 2 in Abbink

et al. (2006). During this phase, the Terschelling Basin was filled with locally more than 2000 m

thick siliciclastic sediments belonging to the predominantly non-marine Schieland Group and the

marine Scruff Group (e.g. Duin et al., 2006). During the third phase, adjacent platforms, like the

Schill Grund and Cleaver Bank Platforms were flooded. This phase, occurring around the

Jurassic-Cretaceous boundary, is referred to as Sequence 3 in Abbink et al. (2006). Sequences 2

and 3 are relatively thick in the Terschelling Basin as compared to the Central Graben. Moreover,

hiatuses occur during Sequence 2 and 3 in the Central Graben, but deposition of Sequence 2 and

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3 was continuous in the depocentre of the Terschelling Basin (Abbink et al., 2006). In the Early

Cretaceous, at the end of the Ryazanian, rifting came to a halt. Fault activity in the Graben area

gradually ceased and the succeeding shallow marine sandstones and shales of the Early

Cretaceous Rijnland Group effectively blanket the former graben and platform areas. From then

on, the southern Graben basin is subjected to thermal subsidence. Because the subsidence is

then no longer limited to the Graben area, it is reflected in a large-scale regional transgression

(Copestake et al., 2003). This “Sequence 4” is referred to as the ‘Cretaceous transgression’ and

starts in the Valanginian.

Sequence 1

Callovian-Oxfordian

Sedimentation of the Schieland Group (Central Graben Subgroup) in the Dutch Central

Graben commenced in the Middle to Late Callovian G.2 (see pdf ) . The sandy fluvial plain

sediments of the Lower Graben Formation covered the erosion surface, mostly consisting of

Lower to Middle Jurassic Altena Group sediments.The upper part of the succession in

particular shows a near coastal marine setting, consistent with the inferred J46 MFS sensu

Partington et al. (1993) from the lamberti Ammonite Zone. The shift to the Middle Graben

Formation in the Early Oxfordian reflects an instantaneous change to more fine-grained,

lacustrine to marginal marine sedimentation. In the southern Dutch Central Graben deposition

started in the Late Callovian with the sedimentation in restricted to shallow marine

depositional environment. These deposits are lithostratigraphically categorised within the

Rifgronden Member of the Friese Front Formation. During the Middle Oxfordian continental

conditions (lower delta plain, lacustrine, lagoonal tidal flats, estuary and tidal channels, bay

head deltas and mouthbars) returned, and prevailed throughout the Dutch Central Graben.

Marine incursions were scarce, and were restricted to the far north during the rest of theOxfordian.

The Bathonian-Callovian Mid-Kimmerian uplift practically terminated the deposition of the

Altena Group in the N etherla nds. Bu t, while essentia lly non-ma rine Schiela nd Group

deposition had already commenced in the Dutch Central Graben, deposition of the Brabant

Formation (Altena Group, Oisterwijk Limestone Member) p ersisted into the Early-Middle

Oxfordian in parts of the Roer Valley Graben and West Netherlands Basin (Haanstra (1963) ;

NAM and RGD (1980) ). These deposits are overlain unconformably by floodplain deposits

(Schieland Group, Nieuwerkerk Formation) of Late Oxfordian to Portlandian age, now

preserved only as erosional remnants.

From the Late Oxfordian onwards, the open marine realm started to expand southwards into

the Dutch Central Graben, first into block F03. Initially, a stacked prograding marginal marine

barrier-island system (Upper Graben Formation) developed, behind which (F08-F14) a paralic

delta-plain setting formed, which is represented by the Puzzle Hole Formation sediments. To

the north of the barrier complex, the Kimmeridge Clay Formation represents the open-marine

environment. The coastal sand-bars of the Upper Graben Formation in the F03-area drowned

at the end of the Oxfordian. Thin coastal-barrier sand-beds are found locally in the uppermost

parts of the Puzzle Hole Formation, suggesting the existence of a backstepping coastal-barrier

system. To the south (F14-F17), the paralic Puzzle Hole Formation grades into a non-marine

(coastal) delta plain facies (Friese Front Formation). Seismic and paleogeographic information

suggests that the transitions from the Puzzle Hole Formation into the Kimmeridge Clay

Formation an d the Friese Front Formation were fault controlled.

Sequence 2

Kimmeridgian

In the northern part of the Central Graben, the Kimmeridge Clay Formation developed further

southwards (F05 Block). Reconstruction of the sedimentation in the Middle Central Graben is

limited due to the Subhercynian/ Laramide inversion in Blocks F08-F17. At the base of Sequence 2 (Late Kimmeridgian) marine deposition (Lies Formation) also flooded into the

northern part of the Step Graben, transgressing deposits of the Zechstein Group. During the

Kimmeridgian, the thus far scattered deposition of the Friese Front Formation in the southern

Dutch Central Graben gradually became more widespread. In Sequence 2 (Late

Kimmeridgian) the Terschelling Basin also opens with fluvial Friese Front Formation deposits.

The depocentre of the Dutch Central Graben axis shifted to the peripheral basins due to a

change in the tectonic regime (see geological history above).

Meanwhile the Broad Fourteens Basin also initiated rifting and widespread deposition

commenced with the sandy fluvial-plain sediments of the Aerdenhout Member from the

Breeveertien Formation (see pdf). It unconformably overlies deposits of the Altena or Upper

Trias Groups.

In the Lower Saxony Basin (= Niedersachsen Basin (see pdf ) ), deposition of the Basal

Weiteveen Clastic Member also seems to have started in Sequence 2.

Early-Middle Volgian

In the latest Kimmeridgian, the first marine influence is shown in the southern Dutch Central

Graben and Terschelling Basin, as testified by the deposition of the shallow marine Oyster

Ground Member (Skylge Formation (see pdf ) ). It is in conformable contact with the underlying

main Friese Front Member. In the Terschelling Basin the Oyster Ground Member may

interfinger with the main Friese Front Member. During the Early-late Middle Volgian a new

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transgression resulted in deposition of the Terschelling Sandstone Member, a foreshore to

shoreface setting grading northwards into the shallow (to open-) marine Noordvaarder

Member (in F15-F17-F18, G.2 (see pdf ) ). These sand dominated successions were

occasionally extensively deposited at the fringes of the Dutch Central Graben (e.g. B14 and

F11).

The distribution of the open marine Kimmeridge Clay Formation is limited to the northern part

of the Central Graben and decreases in size due to the inversion of the Central Graben axis.

The depocentre of relatively open marine clays, had now shifted to the southernmost Central

Graben, southern Terschelling Basin and northern Vlieland Basin (L03-L12; L02-M01) and

refers to the Lies Member.

During this period, the Vlieland Basin was divided into two subbasins, separated by the

Zuidwal volcanic dome (Herngreen, Smit and Wong (1991)). During the late Middle Volgian,

marine conditions prevailed only in the northern subbasin, whereas the southern subbasin

was characterised by terrestrial (lacustrine to lagoonal) deposition.

During the Early-Middle Volgian, clastic deposition in the Lower Saxony Basin was

periodically replaced by precipitation of evaporites and carbonates (evaporitic and marl

members of the Weiteveen Formation (see pdf ) ). These cycles may be correlated with cycles

of coarser and finer clastics, occasionally with evaporites, in the Broad Fourteens Basin

(Breeveertien Formation, several members (see pdf ) ). In the Central Netherlands Basin

(sometimes referred to by the obsolete name ’Voorthuizen subbasin’; Haanstra (1963) ), the

lithofacies (carbonates, marls, evaporites, coal beds) of the Zurich Formation are similar to

those of the Niedersachsen Group.

Sequence 3

Late Volgian-Ryazanian

During the Late Volgian, marine conditions (Scruff Greensand Formation) briefly reached the

entire Vlieland Basin (see pdf ).

In the southern Dutch Central Graben and Terschelling basin the setting became more

shallow, inducing the northward progradation of shallow marine spiculitic glauconite sands

(Scruff Spiculite Member). In the northern Central Graben the basin becomes semi-enclosed

and circulation started to stagnate, resulting in the deposition of bituminous claystones of the

Clay Deep Member (Lutine Formation).

In the Lower Saxony Basin (see pdf ), the Late Volgian shoaling trend is also reflected in as a

hiatus on top of the Serpulite Member within the Weiteveen Formation. At the beginning of the

Ryazanian, the deposition of evaporites and carbonates with minor clastics of the Weiteveen

Formation was replaced by restricted marine to lacustrine deposition of the Coevorden

Formation.

In the Broad Fourteens Basin (Breeveertien Formation (see pdf ) ) this overall regressive

tendency is also reflected by a hiatus (subaerial exposure) between the coastal/fluvial plain

Driehuis Mottled Claystone Member (Sequence 2) and the overlying coastal plain

Bloemendaal Member (Sequence 3) showing brackish water conditions (e.g. in well K18-

Kotter-14: Late Volgian-Early Ryazanian succession is absent).

This period is marked by the resumption of widespread deposition of the Nieuwerkerk

Formation in the Roer Valley Graben and West Netherlands Basin (see pdf ). Thick sequences

of locally coarse fluvial-plain sediments were deposited on rapidly subsiding fault blocks in the

axes of these basins. The depositional realm expanded gradually. Consequently, the basin

margins were covered by only a thin veneer, or remained exposed.

Late Ryazanian

During the Ryazanian the deposition area of the Clay Deep Member (Lutine Formation)

showing stagnant marine circulation in the northern Dutch Central Graben expanded

southward into Block F05 and the Step Graben. The succession of the Lutine Formation

superseded the Scruff Greensand Formation further South in the mid-Ryazanian (see pdf ).

Initially, sedimentation of the Scruff Greensand Formation resumed (Stortemelk Member) and

subsequently succeeded up into the Late Ryazanian of the Vlieland Basin, where this unit is

intercalated with lagoona l/lacustrine de posits of the Zurich Formation. In the Dutch Ce ntral

Graben, differential subsidence gradually stopped by a general decrease of tectonic activity

reflecting the final stages of rifting in the area. A more evenly distributed sedimentation pattern,

associated with the post-rift sag, started. This is shown comparing the highly variable

thicknesses of the sequences underlying the Stortemelk Member with the far more constant

development of the post-rift sequence (Clay Deep Member, Stortemelk Member and Schill

Grund Member). In the Late Ryazanian, mudstone deposition becomes dominant throughout

most of the Dutch Central Graben area.

In the Broad Fourteens Basin, West Netherlands Basin and Roer Valley Graben highly

differential subsidence patterns continued at least throughout the Valanginian.

In the Broad Fourteens Basin the lagoonal Neomiodon Claystone Member slightly

unconformable (K10-event sensu Jeremiah et al., 2010) succeeded the underlying sandy

Bloemendaal Member during the latest Ryazanian.

Sequence 4Valanginian - Barremian

The Late Jurassic rift phase came to an end and coincides with the Cretaceous transgression

(Sequence 4). This occurred by the end of the Ryazanian, albidum Ammonite Zone. The Dutch

area became subjected to subsidence which is reflected in a regional transgression. The

ongoing marine transgression simultaneously reached the Vlieland Basin, Broad Fourteens

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Basin and Lower Saxony Basin, where the first transgressive and coastal-barrier sands of the

Vlieland Sandstone Formation (Friesland, Kotter, and Bentheim Sandstone Members, resp.

G.2 (see pdf ) , G.3 (see pdf ) and G.4 (see pdf ) ) were deposited. Deposition of the

transgressive Kotter Member was followed by the regressive, lagoonal Helm Member

(Breeveertien Formation, G.3 (see pdf ) ), while the Friesland Member in the Vlieland Basin

was followed by open-marine fines of the main Vlieland Claystone Formation G.2 (see pdf ) . In

the Lower Saxony Basin deposition of the Bentheim Sandstone Member was preceded by the

open-marine Bentheim Claystone Member It was followed by the open-marine to lagoonal

Ruinen Member G.4 (see pdf ) .

The advancing transgression caused the Vlieland Basin (see pdf ) to drown during the

Valanginian. The coastline shifted to the Friesland Platform. In the central parts of the Broad

Fourteens Basin (K18-Q01-P03) a stacked coastal-barrier complex was formed (Helder Member). In the central-northern West Netherlands Basin the fluvial Delft Sandstone Member

and lagoonal Rodenrijs Claystone Member are the coastal/fluvial-plain equivalent of the

coastal-barrier complex in the Broad Fourteens Basin. Inland fluvial-plain equivalents are

found in the Roer Valley Graben and southern West Netherlands Basin (Nieuwerkerk

Formation, Alblasserdam Member), and the Central Netherlands Basin and Noord Holland

Platform (Zurich Formation).

The margins of the West Netherlands Basin (L16, P09, Q07) remained exposed until the Late

Valanginian, when the transitional area into the West Netherlands Basin (Q07-Q14) was

flooded. In the Dutch part of the Lower Saxony Basin the Late Valanginian and Early

Hauterivian history is obscured by a hiatus, separating the Ruinen and Westerbork Members

of the Vlieland Claystone Formation G.4 (see pdf ) . This hiatus is also known from other areas,

such as the Vlieland Basin (Herngreen, Smit and Wong (1991) , G.2 (see pdf ) ) and West

Netherlands Basin Haanstra (1963) .During the mid-Hauterivian transgressive phase, an

increasing part of the West Netherlands and Central Netherlands Basins and various platform

areas were incorporated into the marine realm (G.4 (see pdf ) and G.5 (see pdf ) ). The coastline shifted from the Broad Fourteens Basin to the West Netherlands Basin (G.3 (see pdf ) and

G.5 (see pdf ) ), Central Netherlands Basins, Noord-Holland Platform, southern Friesland

Platform and Groningen High, where a sheet of amalgamated transgressive and coastal-

barrier sands was deposited (Rijn Member, Rijswijk Member and Friesland Member of the

Vlieland Sandstone Formation) followed by marine fines (Vlieland Claystone Formation).

On the landward side of the Vlieland Sandstone Formation coastal-barrier system in the West

Netherlands Basin and Roer Valley Graben (Rotterdam area), coastal/fluvial-plain and

lagoonal deposition of the Delfland Subgroup (Nieuwerkerk Formation, Delft Sandstone

Member and Rodenrijs Claystone Member, G.5 (see pdf ) ) con tinued. Minor (restricted-)

marine incursions have been recorded van Amerom, Herngreen and Romein (1976).

Over an increasing area condensed basinal sequences of shallow-marine claystones were

deposited (Vlieland Claystone Formation, G.2 (see pdf ) ). During the Hauterivian, the area of

the marine basin expanded across the northern off-shore, Vlieland Basin, northern Friesland

Platform, Lower Saxony Basin (Westerbork Member of the Vlieland Claystone Formation) andBroad Fourteens Basin. In the Lower Saxony Basin, intercalated sandstone deposits of mid-

Hauterivian age ( Gildehaus Sandstone Member, G.4 (see pdf ) ) reflect a period of coastal

influence in this basin. In the most distal basin areas (Cleaver Bank High, Mid North Sea High)

chalk-like marl deposition set in ( Vlieland Marl Member, G.2 (see pdf ) ).

Barremian

During the Barremian three transgressive-regressive sequences occurred. The first one (latest

Hauterivian-Barremian) formed the Berkel Sand/Claystone and Berkel Sandstone Mbs. G.5

(see pdf ) . Its maximum extension reached slightly further south than the mid-Hau terivian

Rijswijk Member transgression. During the second Barremian transgressive pulse, the

IJsselmonde Claystone and the IJsselmonde Sandstone Mbs. (Vlieland Claystone Formation,

resp. Vlieland Sandstone Formation) were deposited, and the transgression reached the

Rotterdam area. The Nieuwe rkerk Formation realm retreated further south. Main Vlieland

Claystone Formation was deposited on top of the Berkel sandstone complex. At the same

time, the crest of the Texel-IJsselmeer High (see pdf ) was gradually flooded. During the Late

Barremian the area of marine deposition included virtually the entire West Netherlands Basin,

as the Eemhaven Claystone Member (Vlieland Claystone Formation) was deposited. During

the subsequent regressive phase (Late Barremian-Early Aptian), the progradational De Lier

Member (Vlieland Sandstone Formation) was deposited along the south-ern margin of the

West Netherlands Basin.

Not yet classified in terms of sequences

Aptian-Albian

By Aptian and Albian times most of the Netherlands’ territory north of the line O-quadrant -

Breda - Nijmegen was covered by outer-neritic shelf seas G.6 (see pdf ) , reflected in the

widespread Holland Formation. A relatively thin succession of marine marls and claystones

was formed in most places, but in most of the southern Broad Fourteens and West

Netherlands Basins a much thicker sequence, including Holland Greensand Member, was

deposited. Along the southwestern rim of the West Netherlands Basin this open-marine sand

deposit grades into a coast-al-sandstone equivalent (Spijkenisse Greensand Member)

Along the ma rgin of the Lowe r Saxo ny Basin some areas were upli fted dur ing the Al bian

(Coevorden area, also crest of the Texel-IJsselmeer High (see pdf ) ), and the interval in other

areas includes several poorly documented breaks in deposition, related to the (Late Aptian-

Early Albian) Austrian tectonic phase. The deposition of the Holland Greensand Member and

Spijkenisse Sandstone Member in the West Netherlands Basin is also linked to this tectonic

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event. The start of widespread chalk deposition during the Early Cenomanian is taken as the

boundary between the Rijnland and Chalk Groups. In the southern half of the Netherlands the

base of the Chalk Group is placed at the base of the Texel Greensand Member or its

equivalents. The most complete successions of Holland Formation indicate that its deposition

seems to have persisted into the earliest Cenomanian.

Seismic facies

Several seismic examples of each described interval from various structural settings are

included. Different colours have been used in these seismic lines, to discern typical seismic

facies. Each one of these seismic facies represents the typical development of (part of) a litho-

stratigraphic un it, and reflects a specific lithofacies association and de positional setting. It

should be kept in mind that the given sections and their descriptions are not definitions, butexamples. Depending on vintage and processing of seismic data, the described seismic facies

may differ considerably. For the interpretation of the presented examples nearby well

stratigraphies were tied in.

Northern-central Dutch Central Graben:

Figure G7 (see pdf ) displays the seismic facies trend from the northern to the central part of the

Dutch Central Graben. The seismic character of the Upper Jurassic in this province has been

described by Herngreen and Wong (1989) . In the displayed section the following units can be

discerned: Lower Graben Formation: high-amplitude, parallel reflections with relatively low

frequency and medium continuity, characterised by two very high-amplitude, very continuous

reflections. This unit is restricted to fault-controlled depressions.

Middle Graben - Upper Graben Formations:

low-amplitude, high-frequency parallel reflections, very continuous. Because of the low

amplitudes, the unit is virtually transparant. This unit also shows two continuous, very high-

amplitude, parallel reflections at its top. The lower one reflects the base Upper Graben

Formation, while the upper one its contact with the Kimmeridge Clay Formation Towards the

south, where the Upper Graben Formation grades into the Puzzle Hole Formation, the two

parallel reflections diverge as the interval becomes thicker see figure G.9 (see pdf ) .

Kimmeridge Clay - Scruff Greensand Formations:

often very thick, but variable i nterval, mostly low-amplitude, high-frequency reflections of very

high continuity, parallel, divergent, or sigmoidal. Internally repeated trends of increasing

amplitude can be observed. This unit often displays an internal unconformity, downcutting

towards the western flank of the Dutch Central Graben figure G.8 (see pdf ) . In synclines the

top can display a sudden decrease in reflection amplitude. This marks the onset of the Scruff

Greensand Formation Very rarely a thin, transparant interval at the very top of these

occurrences marks the Clay Deep Member or Schill Grund Member of the Kimmeridge Clay

Formation

Puzzle Hole - Friese Front Formations:

package of highly variable thickness, with high amplitude, relatively low frequency, parallel

reflections of moderate to high continuity. This unit represents the Puzzle Hole and Friese

Front Fms. in the southern-central part of the Central Graben. Figure G.7 (see pdf ) clearly

shows how the lateral transition between the Kimmeridge Clay Formation and the Puzzle Hole

Formation was tectonically fixed for a long time, approx. at mark A. At mark B it shows the fault-

controlled transition from the Puzzle Ho le Formation realm to that of the Friese Front Formation

Vlieland Claystone - Holland Formations:

characterised by a very thin package of parallel or wavy reflections of high amplitude, low

frequency and high continuity. Especially the Holland Formation is marked by very high-

amplitude, low- frequency, continuous reflections separated by varying transparant zones.

Southern Dutch Central Graben

Figures G.10 (see pdf ) and figure G.11 (see pdf ) roughly represent the southward continuation

of figure G.7 (see pdf )

Friese Front Formation:

Figure G.11 (see pdf ) demonstrates the loss o f reflector continuity in the Friese Front

Formation towards the south, marking the transition from paralic to fluvial-plain de posits. In

addition, it displays the complex sigmoidal-oblique fill of this basin. Figure G.10 (see pdf )

shows the transparant character of the unconformable, basal Rifgronden Member (lagoonal to

lacus-trine) of that formation.

Scruff Greensand Formation:

Both figures show the southward thinning (convergence) of the Scruff Greensand Formation

This thinning is accompanied by reflectors with increasing amplitude and conti-nuity, and

decreasing frequency. In figure G.11 (see pdf ) an unconformity can be observed at the base of

this unit, and he re only the Stortemelk Member o f the Scruff Greensand Formation is present.

Vlieland Claystone - Holland Formations:

compared to the northern Dutch Central Graben (figure G.7-G.8 (see pdf ) -figure 9 (see pdf ) ),

the Vlieland Claystone Formation is developed thicker here, with a divergent, shingled to

subparallel character. The amplitudes are more varied. Reflections marking disconformities

(sequence boundaries) have higher ampli-tudes. Continuity and frequency remain high. The

thin Holland Formation displays very high-amplitude, low-frequency, continuous reflections

separated by varying transparant zones.

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Vlieland Basin

Figure G.12 (see pdf ) shows the Upper Jurassic-Lower Cretaceous development in the

northern part of this basin.

Kimmeridge Clay Formation:

mildly unconformable, transparent, wavy, moderate to high continuity ( Zurich Formation,

Lower Member in the southern part of the basin.

Scruff Greensand Formation:

interval with lenticular, high-frequency, low-amplitude reflections.

Zurich Formation (Upper Zurich Member):

continuous, high-amplitude, low-frequency reflections.

Vlieland Sandstone

Formation

(Friesland Member):

this unit cuts into the Zurich Formation, and is represented by a sequence of almost

transparant, low-amplitude reflections of fairly high frequency and moderate continuity.

Vlieland Claystone and Holland Formations:

transparent, moderate to hi gh-continuity, high-frequency facies. In this in terval the more

prominent and continuous reflections mark sequence boundaries.

Lower Saxony Basin and Central Netherlands Basin

Not depicted. The Upper Jurassic-lowermost Cretaceous (Zurich Formation or Niedersachsen

Group) is restricted to erosional remnants, such as rim synclines. Seismic facies resemble

those of the Vlieland Basin. A gradual onlap of the Rijnland Group (Vlieland Sandstone

Formation, covered by Vlieland Claystone Formation) is seen. Locally (Coevorden-

Schoonebeek area) the Holland Formation rests unconformably on older rocks, down to

Triassic.

Broad Fourteens Basin

The typical development in this basin can be seen in figure G.13 (see pdf )

Breeveertien Formation (Delfland Subgroup):

is a mildly unconformable, onlapping unit of moderately continuous shingled, divergent or

parallel reflections with moderate to low amplitude and high to low frequency. More

transparent intervals usually represent the claystone members, while sandstone members

tend to show a more pronounced, hummocky character, with many internal truncations.

Vlieland Sandstone Formation:

mildly unconformable, onlapping unit with low frequency, low-moderate amplitude, shingled or

oblique parallel reflections. Towards the east the basal interval grades into a unit of high

amplitude, parallel reflections, formed by the lagoonal Helm Member of the Breeveertien

Formation

Vlieland Claystone Formation:

fairly transparent unit of low amplitudes and high conti-nuity. In some parts reflections have a

higher-amplitude, parallel character.

Holland Formation:

frequently absent in this area, but where present can be thick and tends to have a continuous,

parallel character, with higher amplitudes.

West Netherlands Basin

Figures G.14 (see pdf ) and G.15 (see pdf ) display the western, resp. eastern development of

this basin. The major difference between the two is the structural style. The eastern part is

intensely faulted, and this pattern was already present during the depositon of the Upper

Jurassic.

Nieuwerkerk Formation (Delfland Subgroup):

especially in the lower parts, differential deposition in various fault blocks is important. Seismic

facies of the Nieuwerkerk Formation can be differentiated into two subfacies:

- irregular, discontinuous hummocky clinoforms of moderate to low amplitude (’wormy’ facies),

represent-ing sand-dominated braided fluvial deposits, often showing a mounded character in

downthrown blocks with a thick development (valley fills, see G.15 (see pdf ) ); - a more

transparant facies with some very contigh-amplitude reflections, representing flood-plain or

lacustrine fines, and some intercalated high-sinuosity fluvial intervals.

Vlieland Sandstone and Vlieland Claystone Formations:

comparable to the development in the Broad Fourteens Basin, although considerably thinner

here, as a result of the later start of deposition.

Holland Formation:

thick in the western section, with internal disconformities. The character is comparable to the

Broad Fourteens Basin.

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Structural element Late Jurassic to Early Cretaceous structural

elements

(increase size by clicking on the picture)

Chronostratigraphy Aptian-Albian litho-chronostratigraphic chart

through the Netherlands' territory

(increase size by clicking on the picture)

Late Jurassic - Early Cretaceous (pre-Aptian)

Graben litho-chronostratigraphic chart through

the Broad Fourteens Basin

(increase size by clicking on the picture)

Late Jurassic - Early Cretaceous (pre-Aptian)

Graben litho-chronostratigraphic chart through

the Lower Saxony Basin

(increase size by clicking on the picture)

Late Jurassic - Early Cretaceous (pre-Aptian)

litho-chronostratigraphic chart through the West

Netherlands Basin

(increase size by clicking on the picture)

Late Jurassic - Early Cretaceous (pre-Aptian)

litho-chronostratigraphic chart through the

Vlieland Basin, Terschelling Basin and Dutch

Central Graben

(increase size by clicking on the picture)

References See References Upper Jurassic/ Lower Cretaceous

Van Adrichem Boogaert, H.A. & Kouwe, W.F.P., 1993-1997. [Stratigraphic unit]. In:

Stratigraphic N omenclature of the Netherlands.

D.K. Munsterman, R.M.C.H. Verreussel, H.F. Mijnlieff, N. Witmans, S. Kerstholt-Boegehold &

O.A, Abbink (2012), Revision and update of the Callovian-Ryazanian Stratigraphic

Nomenclature in the northern Dutch Offshore, i.e. Central Graben Subgroup and Scruff Group.

Netherlands Journal of Geosciences-Geologie en Mijnbouw, 91 (4):555-590.

Retrieved [Datum] from [url].

Trefwoorden:

Nomenclator Diep