Late Cretaceous sediment provenance and transfer pathways in...

Late Cretaceous sediment provenance and

transfer pathways in the Faroe Shetland region

September 2007

David W. Jolley

Department of Geology & Petroleum Geology

King's College

University of Aberdeen

Aberdeen

AB24 3UE

UK

Simon Kelley

Department of Earth Sciences

Open University

Milton Keynes

MK7 6AA

UK

Andrew Whitham

CASP

West Buildings

Gravel Hill

Huntingdon Road

Cambridge

CB3 0DJ

UK

Preface

This report is presented in conclusion of the study entitled “Late Cretaceous sediment provenance and

transfer pathways in the Faroe-Shetland region”. Funding from this project was provided by the 'Sindri'

consortium for a group of three projects under the umbrella title

. It forms a part of the Sindri programme 'Future Exploration Issues of the Faroese

Continental Shelf'.The two complimentary projects in this study are are:

Stratigraphy, Sedimentary Provenance

and Sequence Development of the Upper Cretaceous – Paleogene Strata of East Greenland and the Faroe –

Shetland Region

DavidW. Jolley and Simon Kelley

Biostratigraphy zonation (palynology and macrofossil) for the Upper Cretaceous – Lower Palaeogene based on the sedimentary

succession in Kangerlussuaq, southern East Greenland

Developments in the stratigraphy of the pre-basaltic sucession of the Kangerlussuaq basin.Volcanic basins of the North Atlantic:

Integration of data and conclusions

: Phase 1 report by Nohr Hansen, H., Larsen, M. Kelly S.R.A. & Whitham

A.G. 2006.

. Phase III report by Nohr Hansen, H., Kelly S.R.A.,Whitham A.G. Larsen, M. & Jolley, D. 2006.

SUMMARY

Analysis of terrestrial palynofloras from east and west Greenland,offshore Norway and the Faroe-Shetland

Basin has yielded evidence which can fingerprint argillaceous sedimentary sources. Within the region,

phytogeographical analysis has isolated the following types in the Campanian - Masstrichtian interval:

A Norwegian flora, characteristic of this is the combination of triprojectate and Normapolles group pollen

with pollen of laurel types.

A Greenland flora, which contains a moderately diverse triprojectate assemblage, and has a moderately

diverse suite of bryophyte spores.

A Scottish flora,which is characterised by an abundant and diverse triprojectate flora.The remainder of the

assemblage is composed of bryophyte spores,fern spores and gymnosperm pollen,and is not highly diverse.

Within the Faroe-Shetland region, the sediment supply is wholly derived from Greenland. Detrital white

mica dating suggesting it was derived from the Caledonian fold belt,inland in an area now under the ice cap.

Although some Scottish input is identified into the Erlend area, the volumes of sediment derived from this

are minimal.This is a direct contrast to north of 63º, where there is a almost equal input of westerly and

easterly sourced argillaceous sediment into the northeastAtlantic.

Data for the older Turonian Santonian interval is less equivocal, but indicates that the Campanian

Maastrichtian argillaceous sediment transfer model applies here also.

Significant cooling is demonstrated to have occurred in terrestrial environments at the end of the Santonian,

with subsequent warming occurring in the upper Campanian.This provides a stratigraphy for pollen and

spore assemblages in the region, although currently it does not compare with the resolution available from

other micropaleontological data.

In the region of the Faroe Islands a sediment bypass system developed in Santonian - Early Campanian

(Larsen et al., 2005).The new data gathered here indicates that westerly sediment transfer into the Faroe-

Shetland Basin dominated the Late Cretaceous period. Although the lack of borehole coverage means that

direct evidence is not available, sequences of Cenomanian - Coniacian and Late Campanian - Maastrichtian

mudrocks could be expected to occur under the Faroe Islands.There remains the possibility that westerly

sourced clastic sediments of Santonian - early Campanian age may occur in this area.These are more likely to

host arenaceous beds by virtue of them being deposited during a period of low relative sea levels.

The dominance of Greenland sourced argillaceous sediment in the Late Cretaceous Faroe-Shetland Basin to

the exclusion of any easterly source highlights the low lying topography of the Scottish region.With the

initiation of rifting during the Danian,rift flank uplift was initiated and resulted in significant elements of basin

fill being derived from both uplifted flanks.

1

OBJECTIVES

ORIGINS OF NE ATLANTIC PHYTOGEOGRAPHY

This study uses biostratigraphy and phytogeographic analysis of Late Cretaceous sedimentary sections in

Greenland and the Faroe-Shetland Basin to establish the extent of westerly derived sediment influence that

would be expected to occur under the offshore Faroe Islands lava field.This phytogeographical analysis, is

allied to detrital white mica isotopic dating of selected Faroe-Shetland and Greenland (Cenomanian

Maastrichtian) sections.This analysis provides a test and calibration for the phytogeographic data.This will

allow an insight into the likely composition of the Late Cretaceous component of the 2km+ of pre-rift to base

basalt sequence predicted byWhite et al.(2003),for the East Faroe Platform area.

In using palynomorphs to establish sedimentary provenance, it should be borne in mind that pollen behaves

as silt sized particles in the sedimentary system. Transportation of pollen into basinal depositional

environments is dependant on either salinity stratification in the basin watermass,or the location of a plume

or plumes from major sedimentary input points. All of the palynofloras examined were dominated by

(Taxodiaceae redwoods and swamp cypresses) and ( types).

Common occurrences of species are also recorded. These spores are either derived from

mosses or liverworts, suggesting cooler, wet climatic conditions.Their occurrence also maps well onto the

records of macrofossils seem commonly in Campanian Maastrchtian Arctic Canada

(Spicer, pers comm.,2003).

The period from the Campanian to the base of the Palaeocene was one of an overall cooling global climate.

While the Cretaceous - Paleogene boundary was a catastrophic event in terms of the equatorial biota,Arctic

floras show a more gradual change,if any change is evident at all. This change appears to have been,in part due

to the climatic warming initiated at around the K/T boundary, leading to the global greenhouse of the Eocene

Thermal Maximum at 52.5Ma.

Warm climate Palaeocene floras from Greenland are dominated by pollen from what is thought to have been

a mixed mesophytic forest,typified by members of the Fagaceae (Jolley et al.,2005).Occurring with these,are

rare occurrences of pollen, previously only described from North America, implying some connection with

this separate phytogeographic province. A contrasting coeval flora is recovered from Ireland, Hebrides

(Jolley, 1997), offshore Shetland Islands (Naylor et al., 2000; Ellis et al., 2002) and the North Sea Basin (Jolley

and Morton, 1992), being dominated by pollen of the Juglandaceae.The dominant taxa have previously been

recorded as swampland primary colonisers (Wing & Hickey, 1984), and occur along the northeast

Atlantic Margin in association with pollen from other wetland types. Only around the Palaeocene-Eocene

Thermal Maximum (PETM) is this division between Greenland and northeast Atlantic Margin floras broken

down.The thermal maximum forces high latitude warming, which combined with thermal uplift from the

impact of the Iceland Plume under Greenland,creates a land bridge across which elements of floras from the

northeastAtlantic margin,Greenland and NorthAmerica intermix.This ends the trans-Atlantic segregation

of floras,which up to this period had lead to widely different evolutionary pathways in NorthAmerican and

European angiosperms.

The origins of this Early Paleocene floral differentiation lie in the Late Cretaceous (Jolley &Whitham,2004).

The Campanian Maastrichtian was a period of steady climate cooling and falling atmospheric CO levels,

terminating with the K/T boundary event and the subsequent gradual warming of the Palaeocene climate.

Combined with rifting in the NWAtlantic and epicontinental seaways in the NEAtlantic, high sea levels may

have forced segregation of the Arctic flora by marine barriers and a cooling pole. A barrier role is also

probable for the central Asian seaway (Chlonova, 1981). Late Cretaceous plant macrofloras in Alaska and

Siberia show the impact of the isolation of theArctic Ocean from the proto-Pacific,and northward equatorial

warm water transfer along theAmericanWestern Interior Seaway (Herman & Spicer, 1997). These oceanic

barriers would have become increasingly effective as Campanian Maastrichtian temperatures cooled. Plant

microfossil floras recorded from the Late Cretaceous of the circum Arctic have been grouped into the

province,variations in the composition of this providing evidence of the efficacy of the seaway

barriers (Chlonova,1981).

Inaperturopollenites hiatus , Pityosporites PinusStereisporites

'Liverwortiphylum' -

insitu

Aquilapollenites

- 2

-

2

The dominance of the enigmatic angiosperm pollen taxon in the circum Arctic, continued

until the end of the Campanian. From the early Maastrichtian, these triprojectate pollen decline in

frequency, their place being taken by pollen from low diversity,Taxodiaceae (Swamp Cypresses and Dawn

Redwood types) dominated vegetation. While there is some evidence that west Greenland continued to

host an rich flora into the latest Maastrichtian, the decline in their dominance is seen across

the Arctic.This simplification of the Maastrichtian flora is combined with records of Normapolles pollen

(some are proto- Hickories and Pecans) in theseArctic sediments. A small number of taxa from this warmer

Normapolles phytogeographic province are also seen in a mixed Normapolles/Aquilapollenites zone

recorded from western Canada and Siberia. These taxa, and are characteristic

accessories of Palaeocene northeastern Atlantic margin microfloras. Within the Normapolles

phytogeographic province, different species characterise North American and European floras.This is a

reflection of the physical barrier of the North Atlantic, which was re-enforced by the cooling climate. Late

Cretaceous evolutionary pathways within angiosperm groups differed on opposite sides of the Atlantic. In

particular,the Juglandaceae,which form an important part of the northeasternAtlantic margin flora,evolved

from a Normapolles lineage. Other Siberian and western Canadian angiosperm pollen

(?Betulaceae - birches) and (?Myricaceae - myrtles) are also present in the

northeastAtlantic margin and NorthAmerican Palaeocene floras.

Aquilapollenties

Aquilapollenties

,Plicapollis Trudopollis,

Alnipollenites trinaTriatriopollenites triangulus

3

NE ATLANTIC CAMPANIAN - MAASTRICHTIAN PALYNOFLORAS

Sedimentary Provenance

Prior to the commencement of this study, we undertook a research and development project for an

industry partner which has direct relevance to the results presented here. This research involved

palynofloral analysis of the Maastrichtian interval in wells between 63 N and 67 N and the Campanian in a

well from 64 N offshore Norway.This research was undertaken (Jolley, 2004), to determine if any evidence

existed for some of the palynofloras being sourced from the western, Greenland side of the northeast

Atlantic.

Multivariate statistical analysis of the combined dataset from these wells showed significant differences

between the floras. Campanian to Maastrichtian sections in westernmost wells at 64 and 67 had a flora of

moderate diversity, with a suite of triprojectate and Fagaceae pollen similar to that which defines the

Paleocene phytogeography of the Greenland area. The flora of other analysed wells was significantly

different, with an abundance of triporate angiosperm pollen,some of which is of Normapolles affinity.This

is accompanied by a diverse suite of triprojectate pollen taxa. Fagaceous pollen was however lacking in this

assemblage. It was concluded that there are two floras represented in these wells, one of which was

probably derived from Greenland in eastward flowing sediment transportation systems.

When these data are subjected to statistical analysis,a clear division is demonstrated between two types of

Campanian to Maastrichtian flora. The palynofloras of these wells are dissimilar to those recovered from

wells known to have no westerly sedimentary input.

The principle floras are:

1. A Norway derived flora (Figures 1,2).This is of high diversity,with a diverse triprojectate pollen suite

including species not seen in the westerly sourced sediments. It includes diverse Normapolles pollen and

accompanying Lauraceae (laurel) types. The diversity of this flora decreases to the north, reflecting a

lattitudinal lapse in land surface temperature.

2. A westerly, Greenland derived flora (Figures 1,2). This is seen in offshore wells, and in the field

samples examined.There is a moderate diversity of triprojectate pollen,and little or no Normapolles pollen.

These taxa are accompanied by common specimens of and

species (chestnut types).These taxa,only occurring in very low frequencies in the Norway sourced flora,are

characteristic of the Paleocene 'Greenland Flora' (Jolley et al., 2005; Jolley & Morton, 2007).This initial

evidence suggested that the Paleocene 'Greenland Flora' originated prior to the late Campanian.

However, little is currently known about the Late Cretaceous terriginous palynoflora of east Greenland.

Unfortunately, the palynofloral zones determined by Chlonova (1981) for the Late Cretaceous northern

hemisphere, do not correspond with the taxa recorded in these preliminary studies.Analysis of further

Cenomanian to Maastrichtian north-eastAtlantic sections is necessary to establish a more detailed model

for sediment transport.

Recently published seismic interpretations (White et al.,2004) across the Faroe Islands East Faroe Platform

area,have indicated 1-2km thickness of pre-rift to base basalt strata.Isopach data given by these authors also

suggests that the Judd andWestrayTransfer Zones controlled stratal thickness during this Late Cretaceous

Palaeogene period.With the recent discovery of a hydrocarbon system in Quadrant 6004, it has become

imperative to gain an understanding of the sedimentary dispersal patterns in the potential Late Cretaceous

reservoirs of the Faroese area.Currently, there are no wells drilled in Faroese waters which penetrate the

Cretaceous. To circumvent this lack of direct evidence, we will use comparative studies between east

Greenland and the Faroe-Shetland Basin.Using these data,we will interpret sediment distribution pathways

in the Faroese area.

Sedimentary bypass of the Kangerlussuaq shelf by arenaceous sediment may have resulted in deposition of

sediment in the Faroe Islands area. In addition, the unconformity present in Kangerlussuaq between the

Cenomainan-Coniacian (Sorgenfri Formation) and the Campanian-Maastrichtian (Christian IV Gletshcer

Formation) would have shifted the sedimentary system to the basinward side (Whitham et al., 1998).The

stratigraphical interval represented by this unconformity is known to be sand prone in the Nyk High,Vøring

basin. Samples from the Late Cretaceous of wells in this area have recently yielded Greenland derived

terriginous floras. In the Faroe-Shetland Basin, wells penetrating the Cretaceous show that Cenomanian-

Turonian sands are developed on the downthrown side of active faults (e.g. in 206/3-1 to the NW of the

Rona Ridge Fault).Similar,thinner sands are also developed on the top of the Corona Ridge (eg 213/23-1).

° °

°

° °

Cupuliferoipollenites Cupuliferoidaepollenites

4

Vi n

gl e

i a

Structural elements of theNorwegian continental shelfPart II: The Norwegian Sea RegionP . Blystad, H. Brekke, R.B. Færseth, B.T . Larsen, J. Skogseid and B. TørudbakkenPlate I, NPD-Bulletin no. 8 (1995)

70°2° 0° 2° 4° 6° 8° 10° 12° 14° 16°

66°

68°

62°

64°

Målestokk 1 : 1 000 000

BivrostFracture

Zone

Harstad

Basin

Harstad

Utrøst

Ridge

Bivrost Lineament

B odø

Ribban

Basin

NykHig

h

Någrind Syn

cline

Træna

Basin

Naglfar

Dome

S andnessjøen

Halten

Kristiansund

T rondheim

Froan

Terrac

e

Basin

Fault

Magnus Basin

T ampen

Spur

Marulk

Basin

Møre

Sogn

Grab

en

Manet R

idgeSløreb

otnSub

-basin

Trøndela

g

Fault

Gossa

High

ComplexFrøyaHigh

Jan

Mayen

Lineament

Møre

Marginal

High

Hella

ndHa

nsen

JanMayen

FractureZone

Gjallar

GleipneFracture

Zone

Lay-out T .Braanaas, Norsk Hydro, Oslo 1995

PLA TE I

Permo-T riassic basin on the T røndelag Platform

T erraces and spurs

Cretaceous basin on the T røndelag Platform

Platform area and shallow terrace

Cretaceous basins

Cretaceous highs

Palaeogene volcanic, landward side of the escarpment("inner flows")

Marginal highs capped by Palaeogene volcanics

T ertiary domes and arches

Position of profile

Subcrop of top Basement below Quarternary

Subcrop of base Cretaceous below Quarternary

Oceanic magnetic anomaly

Boundary of T ertiary lavas ("Inner flows")

Oceanic fracture zone

T ertiary normal fault

T ertiary volcanic escarpment

Eroded fault escarp

Pre-Jurassic normal fault

Late Cretaceous fault, reactivated normal sense

Late Cretaceous fault, reactivated reverse sense

Late Cretaceous normal fault

Late Jurassic/Early Cretaceous fault, reactivated normal sense

Late Jurassic/Early Cretaceous fault, reactivated reverse sense

Late Jurassic/Early Cretaceous normal fault

Fault polarity not determined

Fault position uncertain

A A'

Figure 1:Map showing the distribution of known palynofloral sources in the NEAtlantic Late Campanian -

Maastrichtian. Pale green arrow = Greenland derived Late Campanian flora; dark green arrow =

Greenland derived Maastrichtian flora. Red arrows = Late Campanian - Maastrichtian Norway derived

floras.Note that this is not an exhaustive map,only showing the extent of the currently available data set.

Basemap after NPD.

5

CA case scores

Axis

2

Axis 1

Inaperturopollenites distichiforme Inaperturopollenites hiatusAlnipollenites verus

Aquilapollenites sum

Cupluliferoidaepollenites liblarensis

Cupuliferoipollenites cing oviformis

Cupuliferoipollenites cingulum fuscus

Deltoidospora adriennis

Expressipollis arcuratus

Kurtzipites sp.

Laevigatosporites haardtii

Lycopodiumsporites spp.

Momipites spp.Nyssapollenites kruschi analepticus

Pseudointegricorpus sp.

Retitricolpites retiformis

Sequoiapollenites polyformosus

Stereisporites (Distanc.) germanicus

Stereisporites (S.) sterioides

Tricolpites hiansTriporopollenites robustus

0.0

0.6

1.7

2.2

2.8

0.00 0.55 1.11 1.66 2.22 2.77

Offshore Norway, Greenland Source, Maastrichtian

Group A: Late successional gymnosperm forest

Group B: Mid successional angiosperm accessory taxa

Group C: early successional bryophyte community

A

B

C

CA case scores

Axis 1

Alnipollenites verus


Baculatisporites primarius

Betulaepollenites microexcelsus

Cicatricosisporites cooksoniae

Cicatricosisporites rousei




Deltoidospora maxoides

Erdtmanipollis sp.

Expressipollis arcuratus

Expressipollis spp.

Fibulapollis mirificus

Gleicheniidites senonicus

Inaperturopollenites distichiforme

Inaperturopollenites dubius

Inaperturopollenites hiatus

Kurtzipites spp.Laevigatosporites haardti


Lycopodiumsporites reticulatus

Mancicorpus notabile

Microfoveolatisporis pseudodentatus

Orbiculapollis sp.

Retitricolpites retiformisSequoiapollenites polyformosus

Stereisporites (Cingulitriletes) sp.

Stereisporites (Distanchorae) germanicus

Stereisporites (Distgranisporites) sp


Tricolpites hians

Trilites multivalatus

Triorites sp

Trudopollis hammenii

Verrucosisporites spp.

Wodehousea sum

0.0

0.8

1.7

2.5

3.4

4.2

0.00 0.85 1.70 2.54 3.39 4.24

Ny

A

B

C

Offshore Norway, Norwegian source Maastrichtian floras

Group A: Late successional gymnosperm/angiosperm forest

Group B: Early successional fern community

Group C: Mid successional angiosperm community

Figure 2: Correspondence analysis plots of Maastrichtian palynofloras from offshore Norway. Note

the greater diversity of the Norway-derived palynoflora. Details of the floral structure will be

discussed below.

6

DATA ANALYSIS

Geographical Society Island

In this section of the report, we briefly describe by area, the sections which have been subjected to

palynofloral or white mica analysis. Ecological analysis of the palynofloras has focussed on

correspondence anlaysis and its derivative, detrended correspondence analysis.These analyses have

beeen undertaken using MVSP software (Kovach, 2002).A discussion of the results and their

implications forms the next section of the report.

Palynofloral analysis of 75 samples from Geographical Society Island, east Greenland, was undertaken to

provide a reference point for the analysis of Late Cretaceous sediments in the Faroe-Shetland Basin (Figure

3 ). Analysis of the pollen/spore component of the palynofloras from the suite of samples from

Geographical Society Island was undertaken to test for the existence of a western sedimentary source into

the offshore Norway region during the Campanian.

The strata from which the samples were collected are the mudstone dominated Knudshoved Member and

sandstone dominated units informally referred to the Leitch Bjerg Member, both belonging to the Home

Foreland Formation (Kelly et al., 1998).These samples had been collected by CASP in 2003 (Whitham &

Kelly,2004),and had subsequently been analysed for their micropaleontological and dinocyst content (Kelly

et al., 2004). Combined with macropalaeontological analysis, data from these studies confirmed a mid

Campanian age for the sedimentary rocks.

Samples analysed for this study were taken from four exposures of Campanian sedimentary rocks on

Geographical Society Island.Two of the sections W4334 and W4342 are up to 300m in thickness and

comprise marine mudstones, sandstones and conglomerates. The remaining two sections, W4355 and

W4356 are thinner, and duplicate parts of the more complete sections, but represent exposure from

further north on the island.

Statistical analysis of Geographical Society Island palynofloras

Multivarite statistical analysis was carried out on the available data set to determine the degree of difference

or similarity between the Geographical Society Island Campanian palynofloras and the Campanian and

Maastrichtican palynofloras from offshore Norway wells. The following results were derived from this

analysis,and illustrated at Figure 4.

Group A: Late successional gymnosperm/angiosperm forestAquilapollenites drumhellerensis





Nyssapollenites kruschi analepticus




Laevigatosporites haardti

Momipites spp

Tricolpites hians

Triporpopollenites/Paralnipollenites con

Baculatisporites primaries



Echinosporis cycloids





Stereisporites (Distanulisporis) spp.

Group B: Early-mid successional angiosperm/fern community

Group C: Early successional bryophyte fern community

7

150 km

Geology (Greenland)

Eocene basalts

Cretaceous

Other rock units

Licence blocks

NW European continent-ocean boundary

East Greenland continent-ocean boundary

Norway wells

Faults

Key

0 150 km

Figure 3:Reconstruction of the Norway-Greenland Sea region at the end of the Paleocene prior to the onset

of seafloor spreading,after CambridgeArctic Shelf Programme (CASP). Green and red arrows show known

Late Campanian - Maastrichtian argillaceous sediment transfer vectors.

72°N72°N

4°E4°E 6°6°

8°8°

10°10°

74°N74°N

66°N66°N

64°N64°N

20°20°22°W22°W 18°18° 16°16°

/

Unclassified

Aquilapollenites spp.Cupuliferoipollenites cingulum pusilus

8

CA case scores

Axis

2

Axis 1

Aquilapollenites drumhellerensis

Aquilapollenites spp.

Baculatisporites primarius



Cupuliferoipollenites cing. pusilus



Echinosporis cycloides



Inaperturopollenites dubius Inaperturopollenites hiatus


Lcopodiumsporites spp.


Momipites spp




Stereisporites (Distanulisporis) spp.


Tricolpites hians


0.0

0.7

1.5

2.2

3.0

3.7

0.0 0.7 1.5 2.2 3.0 3.7

A

B

C

Geographical Society Island, Early Campanian.


Group B: Early - Mid successional angiosperm/fern community

Group C: Early successional bryophyte/fern community

Figure 4: Correspondence analysis of palynofloral data from Geographical Society Island. Note the

similarity in the structure of the groupings between this analysis and that returned for the Greenland

sourced palynoflora in the offshore Norway wells of figure 2.

9

Statistical Analysis of Kangerlussuaq Floras

The Late Cretaceous stratigraphical geology of Kangerlussuaq has recently been clarified by Larsen et al.,

(2005), readers are referred to this report to Sindri for the lithostratigraphical nomenclature used here. In

order to analyze the composition of Late Cretaceous floras in the Kangerlussuaq region of east Greenland,a

number of samples were analysed,taken from field sections collected by CASP (Figures 6-12).

These sections,P2383 ,W4244 ,W4225 (Cenomanian Turonian) andW4275 (mid- late Cenomanian).These

sections are taken from the Sorgenfri Formation (Larsen et al., 2005),which is separated from the overlying

Christian IV Fm by an unconformity encompassing the Santonian to early Campanian interval. Further

palynofloral data was utilised from sections covering the late Campanian to Maastrichtian interval (W4301,

W4268/W4293,W4245 andW4282) within the Christian IV Fm of the same region.

The composite data set from the Sorgenfri Fn sections analysed exhibits a palynoflora of resticted diversity

and abundance. It is dominated by both taxodiaceous pollen and saccate pollen, both derived from

gymnosperms.CA analysis of this palynoflora identifies two main groupings with a succession of outliers, as

with other analyses here, saccate pollen was excluded from the sum as a facies component (Boulter &

Hubbard,1984). The correspondence analysis groupings are (see also Figure 13):

The presence of Cycad pollen in these assemblages is indicative of a frost free temperate climate.

Sorgenfri Fm Sections

Group A: Late Successional gymnosperm forest

Group B: Early-mid successional fern-angiosperm community

Not grouped low frequency and sporadic taxa

Cupuliferoipollenites cingulum fuscusEchinatisporis spp.Expressipollis spp.Inaperturopollenites hiatusKurtzipites spp.Pityosporites spp.Stereisporites (S.) sterioidesRetitricolpites retiformis

Aquilapollenites spp.Concavissimisporites verrucosusDeltoidospora adriennisLycopodiumsporites spp.Tricolpites cf. hians

Caliallasporites turbatusCicatricosisporites cooksoniaeCicatricosisporites rouseiCicatricosisporites spp.Complexipollis sibiricaCycadopites spp.Densoisporites perinatusExpressipollis accuratusGleicheniidites senonicusInaperturopollenites distichiformeInaperturopollenites dubiusKlukisporites spp.Lycopodiacidites spp.Rugosporites bivessicualataStereisporites (Distanchoraesporites) germanicusStereisporites (Distgranisporis) 'granuloidesTriporpopol/Paralnipollenites confususVerrucosisporites spp.

10

KulhøjeKulhøje

SødalenSødalen

Sorteka

pFault

Sorteka

pFault

Cretaceous - Tertiary sediments

20km

Precambrian gneisses

Tertiary mafic and ultramafic plutonic rocks Fault

LocalityTertiary basaltic lavas

Miki Fjord

J.A.D

. Jansen

Fjo

rd

Ryberg

Fjo

rd

Nansen

Fjord

W.4301W.4301

31°31° 30°30°

30°W

68°30’N68°30’N

31°W

W.4218W.4218+

+

+

+

+

+

+ +

SedimentaryMountains

SedimentaryMountains

PyramidenPyramiden

CH

RIS

TIA

I

NVI

GLA

CER

SO

RG

EN

GL

FR

IA

CIE

R

W.4293W.4293

W.4245W.4245

W.4282W.4282

W.4244W.4244+

W.4225W.4225+

+W.4275W.4275

Figure 5: Geological map of the Kangerlussuaq region, eastern Greenland, showing the sample locations

utilised in this study. Modified from CASP original.

+P.2383P.2383

11

3

0m

6

15

18

21

24

27

12

9

Figure 6: Locality P.2383, Sedimentary Mountains, N

Sorg

enfr

iF

orm

ation

Turo

nia

n

S

S

G

G

P

P

M

M

Bed

No

Facie

s

K.11376

K.11377

K.11378

K.11379

K.11380

K.11381

K.11382

K.11383

K.11384

K.11385

K.11386

K.11387

K.11388

K.11389

c

c

c

c

cc

11

22

The diversity of species and the occurrence of other fern spores points to a humid climate,

although the schizacean affinity of the species suggests that there may have been a dry

season. This palynoflora is indicative of warm temperate vegetation of the type suggested by the biome

reconstructions of Chumakov et al. (1995).

CicatricosisporitesCicatricosisporites

Stratigraphical plots of these groupings reveals little change over

the Cenomanian- Turonian interval in the terrestial palynoflora. Frequencies of the early-mid successional

group do occur,but are not of any apparent significance as they exhibit no long term trend.

Cycadopites spp.

Kurtzipites spp.

D adriennis (C)

Expressipollis spp (C)

P infusorioides (C)

H pulchrum

C nyei (C)

I hiatus

Pityosporites spp

with sporadic

Cupuliferoipollenites

and Deltoidospora.

12

C

C

C

C

C

C

C

C

C

Position of lastnodule.

K.10662 P

K.10661 P

K.10660 P

K.10659 P

K.10658 P

K.10667 S

K.10666 S

K.10665 SK.10657 P

K.10664 S

W.4629 S

W.4628 P

dyke

Break of slope

Bench

Bench

Bio decrease upward

Well bio sst

2

3

4

5

6

7

8

9

1010

11

30cm30cm

M S

0 m

10

20

30

40

50

60

70

80

90

100

110

120

130

140

150

Figure 7: Locality W4244, Kangerlussuaq

Impoverished samples

dominated by Pityosporites

and I hiatus

13

Str

ati

gra

ph

ich

eig

ht

85m

80m

75m

70m

65m

60m

55m

50m

45m

40m

35m

30m

25m

20m

15m

10m

5m

0m

Gro

up

So

rge

nfr

iF

orm

atio

nF

orm

ati

on

Lithology Samples

83.00 K10175

81.00 P5474

80.00 K10174

78.00 P5473

77.00 K10173

74.00 K10172

70.50 K10171

66.50 K1119566.00 K1119465.50 K1119365.00 K1119264.50 K1119164.00 K1119063.50 K11189

60.50 K1118860.25 K1016860.00 K1118759.50 K11186

58.50 K1118458.00 K1118357.50 K1118257.00 K1118156.50 K11180

49.50 K10167

47.00 P5444

45.00 P5443

43.00 P5442

41.00 P5441

39.00 K10165

37.00 P5439

35.00 P5437

33.00 K10164

31.00 P5435

29.00 P5433

27.01 P543127.00 K10188

25.00 P5430

23.50 K10162

21.00 P542820.75 K10186-10187

19.00 P5427

17.00 P542616.60 K1018515.50 K1018415.01 P542515.00 K1018114.50 K1018313.30 K1018213.21 K1016013.20 K1016012.71 K1015912.70 K1018011.01 P542211.00 K10178

9.00 P5421

7.00 P5420

5.00 P5419

4.00 K10177

3.00 P5418

0.20 K101570.02 K10191-102160.01 K101570.00 K10157

Figure 8: Location W4225

I hiatus (A), Pityosporites (A),

Deltoidospora (F), G senonicus (F)

Cenom

ania

nTuro

nia

n

14

0 m

10

20

30

40

50

60

C

C

C

C

C

C

C

C

C

C

C

C

C

C

C

C

C

C

C

C

C

C

C

C

C

70

100

110

120

130

80

90

2

3

M S

K.10941 P

K.10942 P

K.10943 P K.10946 SK.10944 PK.10945 S

K.10948 P

K.10947 P

K.10949 P

K.10950 P

K.10951 P

K.11021 P

K.11022 P

K.11023 P

K.11024 P

K.11025 P

K.11026 P

K.11027 P

K.11028

K.11029 P

K.11015 P

K.10940

K.11020 P

K.11016 P

K.11018 PK.11019 S

K.11017

45

6

7

8

9

10

11

650

275

103

Figure 9: Location W.4275, Pyramiden, Kangerlussuaq

Turo

nia

nM

id-

late

Cenom

ania

n

Pityosporites spp (A),

I hiatus (F), Deltoidospora (C)

Cicatricosisporites cooksoniae

I hiatus (C)

15

C

C

C

C

C

C

C

C

C

C

C

C

C

C

C

C

C

C

C

C

C

C

C

C

1

2

3

4

5

6

8

10

9

7

M

K.10564 P

K.10567 P

K.10568 P

K.10569 P

K.10571 P

K.10573 P

K.10574 P

K.10575 P

K.10576 P

K.10586 -94

K.10597 P

cf. Tenuipteria fibrosa

Ophiomorpha

K.10612,3 sp.K.10611 sp.K.10610 sp., sp.,

cf.

GaudrycerasClioscaphitesNautilus Scaphites

Tenuipteria fibrosa

K.10598 P

K.10599 Pabundant redconcretions

K.10600 P

K.10601 P

K.10602 P

K.10603 P

K.10604 P

K.10615 P

K.10616 P

K.10617 P

K.10618 P

K.10607 S.

Teichichnus

S

0

10

20

30

40

50

60

70

80

90

100

110

120

130

C

C

C

C

C

C

C

C

C

C

C

C

C

C

C

C

10

11

12

13

14

15

140

150

160

180

190

200

210

220

230

240

250

170

K.10620 P

K.10621 P

K.10638 PK.10629-34 plants, ,

sp., ,sp., cf.

Diplomoceras cylindraceumSaghalinites Glyptoxoceras indicumPhylloceras Tenuipteria fibrosa

K.10628 SK.10627 S

K.10639 P

K.10640 P

K.10641 P

K.10642 P

K.10643 P

K.10644 P

K.10645 P

K.10647 P

K.10648 P

K.10650 P

K.10651 P

K.10652 P

K.10653 P

K.10654 P

K.10655 P

Diplomoceras cylindraceum

K.10646 S sandstone dyke

dyke [W.2125-18]

Ch

ristia

nIV

Fo

rma

tio

nsill

LA

TE

CR

ETA

CE

OU

S

Early

Maastr

ichtian

Late

Cam

pania

n

Aquilapollenties stelki (C)

Cupuliferoidaepollenites liblarensis& Cupuliferoipollenties cingulum (P-C)

Aquilapollenites clarireticulatusExpressipollis accuratus

Chatangiella spp. (C)

Chatangiella spp.Laciniidinium arcticum

Spiniferites ramosus (C/A)Palaeocystodinium australinum (C)Hystrichosphaeridium tubiferm (C)

Cupuliferoipollenites cingulum (P-C).

Increase in frequency of reworked taxaChatangiella sppCirculodinium hystrix

Palaeoperidinium pyrophorum (C)

Cupuliferopollenites cingulum (C)

Cerodinium deibelii

Increase in frequency of reworked taxaChatangiella sppCirculodinium hystrix

Cupuliferoipollenies cingulum (C)

Cupuliferoipollenites cingulum (F-C)

Laciniidinium arcticum

Sam

ples

analys

ed

Mac

rofo

ssilsu

mm

ary

Palyn

omor

phco

mm

ents

Inaperturopollenites hiatus (A)

Spiniferitesramosus (A)

Figure 10: Location W4245, Sedimentary Mountains, Kangerlussuaq

16

3535

3636

3737

Ma

astr

ich

tia

nT

uro

nia

n/

Co

nia

cia

n

S

S

M

M

85 m

95

100

105

110

115

120

125

90

c

cc

c

c

c

c

130130

3838

3939

4040

4242

4141

P.5481

P.5503

P.5513

P.5494

P.5505

P.5515

P.5496

P.5507

P.5517

P.5477

P.5498

P.5479

P.5509

P.5480

K11350

K11351

K11352

K11353

P.5500

P.5511

P.5492

Circulodinium distinctumOdontochitina operculataChatangiella ditissima

(C)

(start of analysis)

PityosporitesDeltoidospora adriennisCycadopites

spp. (A)(C)

spp.

Laciniadinium arcticum(C)Oligosphaeridium complex (C)

Expressipollis accuratusGliecheniidites senonicusInaperturopollenites hiatus

(F/C)(F/C)(A)

Increase in microplanktondiversity

Aquilapollenites stelkiiA spinulosusFibulapollisTrudopollis hammenii

spp. (F)(F)

Isabelladinium accuminatum

Spinidinium echinoideumFromea fragilisPhelodinium kowolovskii

(F)

?Spiniferites magnificus

Raphidodinium fucatum

Wodehouseia spinata

Triprojectates( )Aquilapollenites clarireticulatus

Chatangiella spp. (C)?Spiniferites magnificus

?Spiniferites magnificus

Chatangiella spp. (F)L arcticum

Odontochitina operculata

HighlyImpoverishedassemblages

Lith

olog

y

Sam

ples

analys

ed

Palyn

omor

phco

mm

ents

Cupuliferoipollenites cingulum(consistant)

Cupuliferoipollenites cingulum(consistant)

Figure 11: Location W.4268/W4293, Sedimentary Mountains, Kangerlussuaq.

17

11

22

33

44

55

66

77

88

99

S G PM

Bed

No

Fac

ies

K.11220

K.11221

K.11227

K.11228

K.11230

K.11232

K.11234

50cm diameterconcretion

K.11225

3

0m

6

15

18

21

24

27

30

33

36

39

42

UnitIIb

UnitIIa

UnitI

45

48

51

12

9

c

c

c

c

c

c

c

c

c

c

c

c

c

c

c

c

1010

1111

UnitIII

Base of Unit III

UnitIIc

UnitIId

c

c

c

c

c

1111

S G P

'Low

er'R

yber

gF

orm

atio

n

Maa

stric

htia

n

'Low

er' R

yber

gF

orm

atio

n

Maa

stric

htia

n

Pos

sibi

lity

ofC

ampa

nian

?

? ?

M

Bed

No

Fac

ies

K.11235

K.11236

K.11237

K.11239

54

57

66

69

72

75

120

123

126

129

Gap of 42m

63

60

1212

1313

1414

1515

1616

K.11240

K.11241

K.11242

Laciniadinium arcticum

Poor or Barren palynofloras

Paralecaniella indentata (F)Inaperturopollenites hiatus (A)

Degraded and thermally mature palynomorphs

Laciniidinium arcticum (F)Momipites? spp.Cupuliferoipollenites cingulum

Cupuliferoipollenites cingulum (F)

K.11243

K.11237

K.11230

K.11220

Figure 12: Location W4301, Sedimentary Mountains, Kangerlussuaq.

18

Similarly, correspondence analysis of palynofloral data from the Campanaian - Maastrichtian Christian IV

Formation sediments has been undertaken. This has produced contrasting results that demonstrate the

occurrence of three main groupings.

Christian IV Formation CA analysis (See Figure 13):

Inaperturopollenites hiatusCupuliferoidaepollenites liblarensisCupuliferoipollenites cingulum fuscusDeltoidospora adriennisMicrofoveolatosporites pseudodentatusNyssapollenites kruschi analepticusPlicapollis pseudoexcelsusStereisporites (S.) sterioides

Expressipollis accuratusGleicheniidites senonicusSequoiapollenites polyformosusStereisporites (Cingulitriletes) spp.Stereisporites (Distanc) germanicusStereisporites (Distverrusporis)Trilites tuberculiformisVerrucosisporitesWodehouseia

Cupuliferoipollenites cingulum oviformisDeltoidospora wolffiEchinatisporitesLaevigatosporites haardtLycopodiumsporitesMonocolpopollenites tranquilisRetitricolpites retiformisTricolpites hiansTrudopollis hamenii

ii

spp.

spp.

spp.

spp,

spp.

Unattributed taxa



Momipites spp.



Group B = Early successional byrophyte community

Group C = Early - mid successional angiosperm/fern community

These groupings show some distinct differences to those derived from the older Sorgenfri Fm palynofloras.

While the late and mid successional communities have overall similarity, there is a lack of thermophyllic

species and normapolles pollen.The spore assemblage is also lacking in the schizacean component seen in

the older palynofloras. However, the main difference arises from the bryophyte dominated early

successional community, which is indicative of a cooler, wetter climatic regime. The stratigraphical and

ecological implications of this change are discussed below

19

CA case scores

Axis

2

Axis 1


AInaperturopollenites dubius

Inaperturopollenites hiatus Cupluliferoidaepollenites liblarensis


Cupuliferoipollenites cingulum oviformis


Deltoidospora wolffi

Echinatisporites spp,

Expressipollis accuratus




Microfoveolatosporites pseudodentatus

Momipites spp.

Monocolpopollenites tranquilis


Plicapollis pseudoexcelsus


Sequoiapollenites polyformosusStereisporites (Cingulitriletes) spp.

Stereisporites (Distanc) germanicusStereisporites (Distverrusporis) spp.


Tricolpites hians


Trilites tuberculiformis

Trudopollis hamenii


Wodehouseia spp.

0.0

1.1

2.3

3.4

4.6

5.7

0.0 1.1 2.3 3.4 4.6 5.7

A

C

Kangerlussuaq, Christian IV Fm field samples


Group B = Early successional byrophyte community

Group C = Early - mid successional angiosperm/fern community

CA case scores

Axis

2

Axis 1


Concavissimisporites verrucosus


Echinatisporis spp.

Expressipollis spp.




Klukisporites spp.

Kurtzipites spp.


Pityosporites spp.


Rugosporites bivessicualata


Tricolpites cf. hians0.0

0.6

1.3

1.9

2.5

3.1

0.0 0.6 1.3 1.9 2.5 3.1


A

B

Kangerlussuaq Sorgenfri Fm field sections:

Group A = Late successional gymnosperm forest

Group B = Early successional fern-angiosperm

Figure 13: Correspondence analysis plots for palynofloras derived from the Sorgenfri Fm Turonian -

Coniacian (top) and from the Christian IV Fm Campanian -Maastrichtian (base).The structure of these

palynofloras is discussed below, but note the occurrence of multiple bryophyte type spores

in the Christian IV Fm assemblages.

Stereisporites

20

Statistical Analysis of West Greenland Floras

Because the data set available for East Greenland is restricted to specific geographical locations, a Santonian

to early Campanian section penetrated by well 6354/4-1 drilled in west Greenland was incorporated into

the study as a comparitor.This has allowed an improved model of paleofloral community structures and their

component taxa to be developed for mid latitude Greenland.Well 6354/4-1 (also known as Quillieq-1) was

drilled by Statoil at W54º 27'06.61” N63º 48' 48.03” within the Fylla East license, offshore central west

Greenland, area to a depth of 2973m (Figure 14).

The petroleum geology of this prospect and the stratigraphical detail of this wel is considered in commercial

reports available through GEUS (Ostby et al., 2001), and the biostratigraphy reported by Nøhr-Hansen et al

(2001).Although the biostratigraphical subdivision of the well section presented by these authors was used in

this study, it was focussed on marine taxa of dinoflagellates, foraminifera and nannofossils.To define plant

communities for comparison with eastern Greenland floras, we analysed the terrestrial component of the

Selandian to Campanian interval of the well.

Ditch cuttings samples from this well yielded an interesting and surprising palynoflora.This flora is dominated

by gymnosperm pollen,and peteridophyte spores,with pollen derived from angiosperms forming only a small

fraction of the assemblages recovered.The characteristic feature of this palynoflora is the abundance and

diversity of the bryophyte spore component,which includes species which are currently not described.It will

be demonstrated here that this bryophyte component is both stratigraphically significant, and represents an

endemic west Greenland floral grouping.

Analysis of the pollen and spore flora from these marine sediments of the 6354/4-1 well was undertaken by

correspondence analysis.Tthe CA analysis again defined clear groupings which have ecological significance.

Group A:Taxodiaceae-fern forest

Group B: Mid succession community

Group C: Bryophyte early successional community

Inaperturopollenites hiatusComplexipollis spp.Deltoidospora adriennisEchinosporis cycloidesGleicheniidites senonicusLaevigatosporites haardtiLycopodiumsporites spp.Nyssapollenites kruschi subsp. analepticusStereisporites (Cingulitriletes) sp.Stereisporites (Distgranisporis) sppTriporpopollenites/Paralnipollenites confusus

Inaperturopollenites dubiusCamerozonosporites insignisCupuliferoipollenites cingulum subsp. fuscusExtratriporopollenites parmatusRetitricolpites retiformisStereisporites (Distanulisporis) spp.Stereisporites (S.) stereioides

Lygodiumsporites spStereisporites (Cingulitriletes) 'spinatus'Stereisporites (Cingulitriletes) 'giganteus'Stereisporites (Distgranisporis) anulatusTrudopollis hemiperfectus

1

21

Group D: Mid successional 222

Group M: Upland

Unclassified

Inaperturopollenites distichiformeCicatricosisporites rouseiExpressipollis accuratusStereisporites (Distanchoraesporis) germanicus

Pityosporites spp.

Dictyophylidites harisiiNudopollis thiergartiiNyssapollenites spp.

Interval of palynological

analysis

Figure 14: Lithological, stratigraphical and electric logs for the 6354/41, after GEUS (2001)

22

CA case scores

Ax

is2

Axis 1




Camerozonosporites insignis


Complexipollis spp.


D adriennis

Dictyophylidites harisii

Echinosporis cycloides


Extratriporopollenites parmatus

G senonicus



Lygodiumsporites sp

Nudopollis thiergartii

N kruschi analepticus

Nyssapollenites spp.


Stereisporites (Cinguli) spinatus

Stereisporites (Cingulitri)giganteus



Stereisporites (Distanulisporis) spp. Stereisporites (Distgrani) anulatus

Stereisporites (Distgranisporis) spp



Trudopollis hemiperfectus-1.2

-2.3

-3.5

-4.7

1.2

2.3

3.5

4.7

5.8

-1,16-2,33-3,49-4,65 1,16 2,33 3,49 4,65 5,82

A

B

C

D

Group A:Taxodiaceae-fern forest community

Group B: Mid successional 1

Group C: Bryophyte early successional

Group D: Mid successional 2

Saccate coniferous pollen was removed from the sum prior to analysis.

Figure 15: Correspondence analysis plot of palynofloras from 6354/4-1, Fylla prospect, west

Greenland. When compared to the Sorgenfri Fm and Christian IV Fm palynoflora CA analyses (Figure

13) it will be noted that this analysis identified two mid successional groups, this is a result of the data

set spanning the Santonian to Campanian interval where palynofloras exhibit a marked change.

Group D is most similar to the mid successional floras identified for the Sorgenfri Fm assembalges,

while Group B is comparable to those determined from the Christian IV Fm data set. The

stratigraphical and ecological inferences drawn from these data are discussed below.

23

Faroe-Shetland Basin

Statistical Analysis of Well 213/23-1 Palynofloras

Having analysed the composition of the terriginous palynoflora from Greenland, and discussed the rather

more diverse flora derived from Norway, this section reports the analysis of Late Cretaceous palynofloras

from the Faroe-Shetland Basin.The results of the palynofloral analysis are presented below,under individual

well headings.

This well was drilled on the edge of the Corona Ridge (Figure 16) on the UK side of the Faroe Shetland Basin,

penetrating a thick sequence of mudstones between the base of the Paleocene (3099m) to the top of the

Cenomanian at 3489m. The well completed in basement below 4342m. The following Late Cretaceous

sequence was identified:

Late Paleocene: 2987m - 3099m

Unconformity

Campanian 3099m - 3126m

Coniacian 3126m - 3250m

Turonian 3250m - 3489m

Cenomanian 3489m - 3578m

**

Blosseville Kyst

Kangerlussuaq

GREENLAND

FAROE ISLANDS

SHETLAND

Faro

e-Sh

etlan

dBa

sin

Victory

Clair

WestrayJudd

Erlend

East

Faro

eH

igh

Cor

ona

Rid

ge

*209/3-1*209/4-1

219/21-1

Coro

naBas

in

B

AA Foinaven Sub-Basin

B Flett Sub-Basin

12

3

4

Igneous centres

1 West Erlend

2 East Erlend

3 Brendan’s Dome

4 Ben Nevis

5 Westray

5

* Well location

Wes

t Shet

land

Platfo

rm

*213/23-1

ErlendPlatform

Structural high

Exposed lava succession

(Greenland)

MorayFirth

Area ofmain map

Skye

Scotland

Figure 16: Location map of Faroe-Shetland basin wells analysed for this study

24

Group A: Late successional gymnosperm/fern forest

Group B: Early successional fern/angiosperm community


Unattributed

Inaperturopollenites ditichiformeInaperturopollentiee hiatusApendicisporties spp.Cicatricosisporites rouseiCupuliferoipollenties cingulum pusillusDeltoidospora adriennisLycopodiumsporites spp.

Cupuliferoipollenites cingulum pusillusCupuliferoidaepollenties liblarensisLaevigatosporites haardtiiMonocolpopollenties tranquilusAquilapollenties sum

Baculatisporites spp.Concavissimisporites verrucosusCycadopites spp.Deltoidospora concavusDeltoidospora wolfiiEchinatisporis spp.Gleicheniidites senonicusStereisporites (Cingulitriletes) spp,(Stereisporites (Distgranisporis) spp.Stereisporites (Distanchoraesporis) spp.Stereisporites (Stereisporites) sereioides

Cupuliferoipollenites cingulum oviformisNyssapollenites kruschii analepticus

This well section is one of the longest stratigraphical intervlas studied, spanning the period fromTuronian to

Maastrichtian.Although the palynofloras of the Maastrichtian are somewhat impoverished,particularly in thes

upper section, recovery increases downhole, allowing the identification of a bryophyte based early

successional community, similar to that seen in the Campanian-Maastrichtian of eastern Greenland.

Correspondence analysis of the Late Cretaceous palynofloras from well 213/23-1yeilded a three-fold

division (Figure 17):

25

CA variable scores

Axis

2

Axis 1

Inaperturopollenties distichiformis

I hiatus

Appendicisporites

Aquilapollenites Sum

Baculatisporites

C verrucosus


Cupuliferoidaepollenites liblarensis

C cingulum oviformis

C cingulum fusus

C cingulum pusillus

Cycadopites


Deltoidospora concavus

D wolfii

Echinatisporis spp

G senonicus

L haardtii

Lycopodiumsporites spp

Monocolpopollenites tranquilus

N kruschii analepticus

S(Cingulitriletes) sp

S (Distgranisporis) spp

S(Distanchoraesporis) sppS(S) stereiodes

-0.9

-1.7

-2.6

0.9

1.7

2.6

3.4

4.3

-0,85-1,70-2,55 0,85 1,70 2,55 3,40 4,25

A

CB

Maastrichtian - Turonian 213/23-1

Group A: Late successional gymnosperm/fern forest

Group B: Early successional fern/angiosperm community


Figure 17: Correspondence analysis of terrestral palynofloras from 213/23-1

CA case scores

Axis

2

Axis 1





Kurtzipites spp.

Laevigatosporites haardtii

Lycopodiacidites spp.



Pseudointegricorpus spp

Stereisporites (Stereioides) spp.

-0.9

-1.7

0.9

1.7

2.6

3.4

4.3

-0,85-1,71 0,85 1,71 2,56 3,42 4,27

Turonian - Maastrichtian interval Well 209/4-1A


Group B: Early successional angiosperm/fern community

Group C: mid successional accessory taxa

AB

C

Figure 18: Correspondence analysis of terrestrial palynofloras from well 204/9-1A.

26

Statistical Analysis of Well 204/9-1A Floras

Statisical Analysis of Well 219/21-1Floras

This well was drilled in 1984 on the north flank of the Erlend volcanic complex. After drilling through

Paleocene volcanic rocks, the well penetrated Maastrichtian strata at 3120m (10130’ ), with Cretaceous

sedimentary rocks being encountered toTD.

Maastrichtian 3120m - 3246m

Early Campanian 3246m - 3367m

Coniacian 3367m - 3810m

Middle to Late Turonian 3810m - 4049m (TD)

Correspondence analysis of the palynofloras recovered from this interval derives three groups(see

Figure 18):

Group C is, in part, a stratigraphical grouping caused by the high levels of and

species in the Campanian.The triprojectates grouped under the genus ,should most probably

be attributed to this group, but they are found commonly in the Coniacian and Turonian section, possibly

augmented by cavings from the overlying interval.The late successional forest,GroupA, is one composed of

Taxodiaceae-Nyssaceae and accessory polypodiaceous ferns and is closely similar to those seen in other

localities. The early successional angioserm fern community is dominated by ferns ( and

) which characterise much of Late Cretaceous floodplain temperate vegetation.This grouping

is particularly well represented in theTuronian - Coniacian interval for reasons discussed below.

This is the most recently drilled of the studied wells,being drilled on the Ben Nevis prospect to the south east

of the Brendan’s Dome igneous complex (Figure 16).The stratigraphical subdivision of the section is largely

based upon the operator’s end of well report, as the palynofloras recovered are in many cases impoverished.

In this study,the microplankton palynoflora was only of significant stratigraphical value in the older part of the

Cretaceous interval,much of the Campanian - Maastrichtian section yielding only terrestrial palynofloras.

Late Maastrichtian 1985m - 2069m

Early Maastrichtian 2069m - 2139m

Maastrichtian/Campanaian 2139m - 2154m

Campanian 2154m - 2319m

?Santonian 2319m - 2404m

Correspondence analysis of the palynofloras recovered from the Late Cretaceous interval derives a poorly

defined result.This is in part attributable to the barren or impoverished nature of many of the samples.

Unconformity

Unconformity

Pseudointegricorpus KurtzipitesAquilapollenties

DeltoidosporaGleiceheniidites


Inaperturopollenites hiatusLaevigatosporites haardtiiNyssapollenites kruschi analepticus

Group B Early successional gymnosperm forest

Group C: Mid successional fern/angiosperm community

Aquilapollenites spp.Deltoidospora adriennisGleicheniidites senonicusStereisporites (Stereioides) spp.

Kurtzipites spp.Lycopodiacidites sppLycopodiumsporites spp.Pseudointegricorpus spp

27

What is derived from this analysis can be interpreted as one single group comprising

The two triprojectate genera, and are recorded as outliers from this main

grouping, and possibly represent secondary vegetation (Figure 19)

Inaperturopollenitess hiatusDeltoidospora adriennisCupuliferoipollenites cingulum fususStereisporites (S.) Sterioides

Mancicorpus Aquilapollenties

CA case scores

Axis

2

Axis 1







-1.4

-2.9

1.4

2.9

4.3

5.8

7.2

-1,44-2,88 1,44 2,88 4,31 5,75 7,19

Figure 19: Correspondence analysis of Late Cretaceous terrestrial palynofloras from well 219/21-1.

28

PHYTOGEOGRAPHICAL ANALYSIS

StratigraphicalVariation

This section is divided into two parts, one concerning stratigraphical variation in the palynofloras from

around the north-east Atlantic, the second examining the inter-regional variation within these floras.

Results from the correspondence analysis have demonstrated variation in the composition of some of the

Late Cretaceous palynofloras analysed here.This is demonstrated in single sections which span theTuronian

to Maastrichtian interval.

209/4-1A

0%

20%

40%

60%

80%

100%

10130.0

10150.0

10200.0

10250.0

10350.0

10400.0

10450.0

10750.0

10800.0

10850.0

10950.0

11100.0

11190.0

11300.0

11350.0

11410.0

11450.0

11500.0

11550.0

11600.0

12200.0

12820.0

Mid

su

cce

ssio

na

la

ng

iosp

erm

s

Ea

rly

su

ccce

ssio

na

la

ng

iosp

erm

/fe

rn

La

tesu

cce

ssio

na

lg

ym

no

sp

erm

fore

st

6354/4-1

0%

20%

40%

60%

80%

100%

19

41

.0

19

80

.0

20

22

.0

20

91

.0

21

30

.0

21

51

.0

21

81

.0

22

20

.0

22

41

.0

22

71

.0

22

92

.0

23

13

.0

23

31

.0

23

52

.0

23

70

.0

23

91

.0

24

12

.0

24

51

.0

24

90

.0

25

32

.0

25

71

.0

26

10

.0

26

31

.0

26

52

.0

26

73

.0

27

03

.0

27

24

.0

27

60

.0

28

11

.0

28

50

.0

28

92

.0

29

31

.0

Mid

successio

nal2

Bry

ophyte

early

successio

nal

Mid

successio

nal1

Taxodia

ceae-f

ern

fore

st

213/23-1

0%

20%

40%

60%

80%

100%

10170.0

10190.0

10210.0

10230.0

10250.0

10270.0

10290.0

10310.0

10330.0

10350.0

10370.0

10390.0

10410.0

10430.0

10450.0

10470.0

10490.0

10550.0

10570.0

10590.0

10610.0

10630.0

10650.0

10670.0

10690.0

10710.0

10730.0

10750.0

10770.0

10790.0

10810.0

10830.0

10850.0

10870.0

10890.0

10910.0

10930.0

10950.0

10990.0

11010.0

11030.0

11050.0

11100.0

11120.0

11150.0

11170.0

11190.0

11220.0

11240.0

11260.0

11300.0

11320.0

11340.0

11360.0

11380.0

11400.0

11420.0

11440.0

11450.0

Ungro

uped

Early

successio

nalbry

ophyte

/fern

com

munity

Early

successio

nalfe

rn/a

ngio

sperm

com

munity

Late

successio

nalgym

nosperm

/fern

fore

st

San

tonia

n

Conia

cian

Ear

lyC

ampan

ian

Maa

stri

chtian

Conia

cian

Turo

nia

n

Fig

ure

20:C

orr

ela

tion

pan

elofw

ells

6354/4

-1(W

est

Gre

enla

nd),

209/4

-1A

(Erl

end

Com

plle

x)

and

213/2

3-1

(Coro

na

Rid

ge),

show

ing

the

norm

alis

ed

stra

tigr

aphic

aldis

trib

ution

ofth

em

ajor

eco

logi

calgr

oupin

gsid

entified

inth

epal

ynoflora

s.Sac

cate

conifero

us

polle

nhas

not

been

plo

tted

beca

use

ofth

edis

tort

ion

inth

eva

riat

ion

ofoth

er

groups

that

isca

use

dby

its

incl

usi

on.

29

Within well 6354/4-1 it is evident that there is a fundamental difference between the Santonian and

Campanian palynofloras. The abundance of early and mid successional communities increases upsection,

implying that there is increasing disturbance to plant community structure through the latest part of the

Santonian and in the Early Campanian.This is supported by the high frequency of such communities in the

records from the Campanian of Geographical Society Island and Kangerlussuaq in east Greenland. A similar

pattern is observed in 213/23-1 where the early successional fern/angiosperm community increases into the

Campanian.This shift in composition is most pronounced in well 209/4-1A where an influx of triprojectate

pollen within the base of the Campanian results in increased proportions of secondary vegetation

communities.

Most probably occurring within the base of the Campanian is a second, connected change in the composition

of the palynofloral communities recorded here.This is most marked in 6354/4-1,but is also evident between

the Kangerlussuaq data sets from the older Sorgenfri Fm and the younger Christian IV Fm.This change

comprises a marked increase in the abundance of bryophyte spores ( species), their frequency

allowing the recognition of bryophyte dominated communities.Within Greenland, this change is consistent,

but there are remarkable differences in the proportions and species of bryophytes from the west to the east.

The westerly section seen in well 6354/4-1 contains a diverse suite of bryophyte spores, including some

undescribed taxa, taxa which do not occur in the Kangerlussuaq or Geographical Society Island. The

Campanian vegetation represented by this palynoflora is one dominated by gymnosperms with associated

ferns and some angiosperm taxa. The majority of the early successional vegetation was composed of

bryophytes,suggesting that a comparison with modern dayTaiga (Figure 21).

Stereisporites

Figure 21: Modern Taiga vegetation, south of the Brooks Range mountains,Alaska.The vegetation in the

background is formed of black spruce ( ),whilst the foreground area is recovering from one of the

frequent forest fires and is covered by alders ( ), willows ( ) and birches ( ).The herbaceous

angiosperms that dominate the foreground had not evolved to this form in the Late Cretaceous, their place

being taken by ferns and bryophytes.

Picea nigraAlnus Salix Betula

This Taiga type vegetation replaced the Santonian and older vegetation that contains early and mid

successional communities dominated by ferns.These ferns are relatives of a range of modern cool to warm

temperate families, and some that imply the potential for seasonal dry periods (Schizaceae). In addition to

these ferns are early angiosperms belonging to the Normapolles group,and frost sensitive taxa such as cycads.

These plants grew in association with a redwood/swamp cypress dominated forest vegetation.

30

This kind of vegetation, in which angiosperms occur within the late early successional and mid successional

communities, is seen in the Santonian section of 6354/4-1, the Sorgenfri Formation of Kangerlussuaq and in

the Turonian - Coniacian interval of the Faroe-Shetland Basin wells.The late successional vegetation has no

direct parallel today, but the temperate fern dominated mid successional vegetation is still evident in areas

where scrubby angiosperms have not displaced them (Figure 22)

Figure 22: Something of the appearance of riparian fern dominated vegetation in the Turonian - Santonian

can be gained from this assemblage of (background) and (a floating water fern).Dicksonia Azolla

Such a fundamental change in community structure provides a valuable ecological and stratigraphical marker

event, but to assess the importance of this event, it is necessary to identify the cause. In this case, there is

already significant evidence pointing towards changes in post-Coniacian plant community structure being

attributable to climate deterioration after the mid Cretaceous optimum. Data supporting this is largely

derived from plant macrofossils, utilizing the coarse-scale mapping of climatically sensitive plant and

lithological data (Spicer & Parrish, 1990; Chumakov et al., 1995).The mean annual temperature (MAT) data

produced from analysis of plant macrofossil assemblages (Spicer & Parrish, 1990) indicates a fall of 8°C

between the mid Coniacian and mid Campanian for floras from Alaska.The data presented here is from the

same biome and climatic belt as the Alaskan data of Spicer & Parrish, and is therefore directly comparable.

Such a fall in MAT would be sufficient to change the vegetation structure from a temperate gymnosperm-fern-

angiosperm forest to a conifer and bryophyte dominated Taiga (Wolfe, 1981). These data presented here

demonstrate, for the first time, that this cooling caused a significant change in the regional vegetation by the

start of the Campanian.

By examination of Figure 19, it will be noted that the representation of the bryophyte community declines to

the end of the Campanian in well 6354/4-1.There is a further change in the palynoflora that is not immediately

apparent from this figure, that is one of increasing abundance of the genus in the early

Campanian above 2130m.

Cupuliferoipollenties

31


Cupuliferoipollenties

becomes the dominant taxon in the Mid successional 1 grouping,an increase in abundance

also seen in the coeval Christian IV Fm data set from Kangerlussuaq.This is of phytogeographical significance,

as this genus becomes one of the characteristic features of the transported ‘Greenland Flora’ recorded in

westerly sourced sediments from the Paleocene Faroe-Shetland Basin (Jolley et al., 2005, Jolley & Morton,

2007). Such an increased representation of occurs at the expense of bryophyte spores,

these changes suggesting that the palynoflora represents the gradual warming of the climate during the

Maastrichtian.These data support the conclusion of Jolley & Whitham, (2004), that the origins of northeast

Atlantic Paleocene phytogography lie in the Campanian - Maastrichtian.

This variation will be considered in two stratigraphical intervals, Campanian - Maastrichtian and Turonian -

Santonian.

It is worth reiterating the differences stated earlier between the Maastrichtian-Campanian floras of Norway

and Greenland

Inter Regional Variation

Campanian - Maastrichtian

The principle floras are:

1. A Norway derived flora which is of high diversity, with a diverse triprojectate pollen suite including

species not seen in Greenland sediments.It includes diverse Normapolles pollen and accompanying Lauraceae

(laurel) types. The diversity of this flora decreases to the north, reflecting a decline in land surface

temperature.

2. A westerly,Greenland flora. This is seen in offshore wells,and in the field samples.There is a moderate

diversity of triprojectate pollen,and little or no Normapolles pollen.These taxa are accompanied by common

specimens of and species (chestnut types). These taxa, only

occurring in very low frequencies in the Norway sourced flora,are characteristic of the Paleocene 'Greenland

Flora'.

So how do these two floras differ from that of the Faroe-Shetland area?

In a previous Sindri study, Larsen et al., (2005) presented an environmental reconstruction of the Faroe-

Shetland region during the Campanian. Because of high relative sea levels and limited extension of the Late

Cretaceous NE Atlantic basin, coarser clastic sediment became ponded on the shallow marine shelf to the

northwest, now forming eastern Greenland. These authors suggest that the evidence of silicified chalk

deposits as far north as Skye (Mortimore et al., 2001,) indicates that chalk deposition once extended over

much of the Scottish mainland, implying minimal sediment supply from the basins eastern flank. Larsen et al.,

(2005) surmise that the large thicknesses of Campanian - Maastrichtian mudrocks found in the Faore -

Shetland Basin must have been sourced from Greenland to the northwest,with limited arenaceous input from

an emergent Shetland Islands area,and from the core of the highland Scottish mainland not submerged by the

high relative sea level.

In considering the Larsen et al., (op. cit.) model, it is important to give consideration to the preservation of

?Campanian - Maastrichtian shallow marine quartz arenites on the mainland adjacent to the isle of Mull.

Locally termed the Loch Aline Sandstone, these sediments are preserved above the Griburn Chalk on Mull

itself and reported as‘desert sandstones’ by Bailey et al.(1924).These deposits suggest that the shallow region

from the Hebridies to the Shetlands may have been a sediment starved shallow marine arenaceous shelf,

rather than a carbonate platform. However, sediment supply from this environment into the deeper basin

would have been negligable.

Testing this model of sediment transport is straightforward using the palynofloral data set contained in this

study. If the majority of Faroe-Shetland Basin mudrocks are sourced from Greenland,this will be evident from

a close affinity between floras derived from Faroe - Shetland wells,and those from Kangerlussuaq. Accordingly,

a data set was assembled from the Campanian - Maastrichtian samples from Kangerlussuaq,and wells 213/23-

1 (Corona Ridge) and 209/4-1A (Erlend Complex).This data set was subjected to correspondence analysis

(Figure 23),which identified a close similarity between the palynofloras of Kangerlussuaq and those of 213/23-

1.Well 219/21-1 is unfortunately barren of palynomorphs in the Campanian - Maastrichtian interval, but well

209/4-1A displays a clearly different palynofloral composition.

Cupuliferoipollenites Cupuliferoidaepollenites

32

CA variable scores

Axis

2

Axis 1

A

BC

D

E

FG

H

I

JK

1

2

3

4

10650

10648

10647

10645

10644

10643

10642

10641

1062910616

10615

10604

10603

10602

10601

10579

10584

10576

10575

10571 11237

4690

-1.1

1.1

2.3

3.4

4.5

5.7

-1,14 1,14 2,27 3,41 4,54 5,68

CA variable scores

Axis

2

Axis 1

Aquilapollenties sum

Baculatisporites spp.

Concavissimisporites verrucosus



Deltoidospora wolffi

Echinatisporites spp,






Kurtzipites spp.


Lycopodiacidites spp.


Momipites spp.

Monocolpopollenites tranquilis

Plicapollis pseudoexcelsus


Pseudointegricorpus spp

Stereisporites (Cingulitriletes) spp.

Stereisporites (Distanc) germanicus

Stereisporites (Distverrusporis) spp.


Tricolpites hians


Trilites tuberculiformis

Trudopollis hamenii


-0.7

-1.3

-2.0

-2.7

0.7

1.3

2.0

2.7

3.3

-0,66-1,33-1,99-2,65 0,66 1,33 Nyssapoll.Microfoveolatisp.

Figure 23: Detrended correspondence analysis plots of samples (top) and species (bottom) from the

selective data set for the Campanian - Maastrichtian palynofloras of Kangerlussuaq and the Faroe-Shetland

Basin. Note that samples from well 213/23-1(green triangles) plot with the Kangerlussuaq samples (blue

triangles).Samples from 209/4-1A (red triangles) plot in a completely separate field.In the species DCA plot

below, species characteristic of the Erlend area wells plot away from shared and Kangerlussuaq/Faroe

Shetland Basin samples.

Erlend specific taxa

Greenland sourced

Taxa

33

This difference in composition is reflected in the community analysis (Figure 20), the species composition

(Figure 23) and the sample similarity (Figure 23),providing clear evidence for a different argillaceous sediment

source for the Erlend area during the Campanian - Maastricthtian period.To test this result, data gathered by

Jolley & Bell (2002) from the centre of the Erlend Complex in well 209/9-1 was examined,and the data derived

from Campanian siliciclastic sediments extracted into the table below,taxa with single specimen occurrences

and saccates being excluded.

sum 2 23 28

0 1 2

14 23 8

spp. 0 2 3

3 9 5

0 2 0

2 5 3

0 2 2

0 0 2

spp. 1 6 7

Well 209/9-1 additional extracted palynology data.Single occurrences and are excluded from these data.

Depth(m) 1508.0 1661.0 1664.0

AquilapollenitesDeltoidospora adriennisInaperturopollenites hiatusKurtzipitesLaevigatosporites haardtiiMonocolpopollenites tranquilisNyssapollenites kruschi analepticusStereisporites (Stereisporites) steroidesStereisporites (D.) germanicusPseudointegricorpus

Pityosporites

These data show a close similarity to that derived from well 209/4-1A to the north, suggesting that this

triprojectate-dominated palynoflora was characteristic of a sediment source derived from the north of the

Shetland area during the Campanian - Maastrichtian.

A similar approach to that adopted for analysis of phytogepgraphic provincialsim was adopted for analysis of

data gathered from the Turonian - Santonian interval. Although older, this interval is thought to have been

deposited under similar marine conditions to that of the Campanian - Maastrichtian interval studied above.

Relative sea levels at this time were high, with mudstone deposition mantling the Faroe Shetland Basin,

resulting in Greenland sourced muds being deposited across the area. Later a major regression forced an

unconformity at the margins of the basin, spanning the Santonian to Early Campanian.This unconformity has

been used to separate theTuronian to Santonian data set from the Campanian-Maastrichtian data.

Results from the CA treatment of the combined data set are presented at Figure 24,and demonstrate a clear

separation between samples from well 209/4-1A and those from all the other study data included.This is

supported by the species CA scatter plot which shows a clear separation of the triprojectate rich flora of

209/4-1A from the dominantly gymnosperm-fern flora of the other sites.Although the nature of the ditch

cuttings samples in 209/4-1A means that there may be some element of cavings in this well from the overlying

interval, there remains the possibility that the mudrocks present in the Turonian-Coniacian of this well are

derived from a Shetland source area.

Unfortunately,other wells drilled in this region do not provide a means of testing the Shetland source in 209/4-

1A, because they TD in younger strata. Because of this, it is necessary to assign some caution to the

observations of Turonian-Santonian sediment derivation,regarding a Shetland source as possible in the Erlend

area.

Turonian - Santonian

34

DETRITAL MUSCOVITE ANALYSIS

AnalyticalTechniques

Laserprobe Ar/ Ar results

Detrital muscovite grains were separated from ditch cuttings of sandstones and siltstones by crushing and

hand picking under a binocular microscope. For samples from well 219/23-1 well, around 25-50 clean white

mica grains,generally greater than 250 microns diameter were picked and cleaned ultrasonically in methanol

and de-ionised water prior to packaging in aluminium foil. For the Kangerlussuaq samples, as many samples

were extracted as possible from the cuttings prior to cleaning, however in many cases, samples were

consolidated in order to create sufficient sample.All samples were irradiated in the McMaster (Canada)

reactor for 50 hrs and the neutron flux was monitored using GA1550 biotite standard (98.79±0.96 Ma,

(Renne ,1998)). On return, the micas were loaded into 2 mm diameter holes an aluminium platen such

that individual grains could be targeted.Argon isotopes data were obtained on individual detrital muscovite

grains by total fusion of individual grains using a spectron 902TQ CW Nd-YAG laser focussed through a

customised Leica microscope. Gasses released by laser fusion were cleaned by two Zr-Al getters for five

minutes prior to automatic inlet into an MAP 215-50 noble gas mass spectrometer,where all masses from 35

to 41 were measured. Analyses of Ar to Ar were corrected for blanks measured either side of two

consecutive samples analyses, 37Ar decay and neutron-induced interference reactions. Argon isotope data

for individual grains are shown in Appendix 2,

The ages of 69 detrital white micas were measured in Cenomanian/Turonian sediments from Kangerlussuaq,

and 125 detrital white micas were analysed from sediments recovered from a well in the Ben Nevis area of

the Faroe-Shetland Basin (219/21-1). Individual ages from Kangerlussuaq ranged from 307-2391Ma, while

those from the Faroe-Shetland area ranged from 894-980Ma.

Samples from Cenomanian/Turonian in Kangerlussuaq are shown in Figure 25 The most striking feature is

the mode (425Ma) in caledonian mica ages with a tail of older ages ranging up to 2391Ma. This is very similar

to other detrital mica signatures in Cretaceous sediments from southern Greenland,and the Faroe-Shetland

basin.

et al.

36 40

40 39

table 1 and table 2.

.

0 500 1000 1500 2000 2500

Rela

tive

pro

bab

ilit

y

36

Sample Well Depth(feet) Age Lithology

P5403 205/10-3 (4) 8456.5 Top Maastrichtian Mud

P5406 214/27-1 (4) 16491.75 Upper Maastrichtian Mud

P5408 219/20-1 (2) 12347.5 Campanian Mud

P5409 219/20-1 (6) 15982.0 Cenomanian-Turonian Mud

Figure 28 shows the results from two Cenomanian/Turonian samples which indicate a similar age distribution

to the samples analysed here. In addition,upper Maastrichtian samples yield the dominantly caledonian signal

seen in Kangerlussuaq. This pattern reflects the dominant supply of this area via supply pathways during the

Campanian/Mastrichtian). In contrast Paleogene samples in the Faroe Shetland basin contain a much higher

proportion of Proterozoic micas, and are less dominated by caledonian micas, a feature we can track using

matching reworked palynomorphs and indicates polyphase C

(unpublished data and Jolley & Morton,2007).

Although there are fewer Cenomanian/Turonian and Campanian/Maastrictian samples from the basin, the

changing pattern is clearly identical to that seen in Kangerlussuaq. The implication of this similarity is that

argillaceous sediment deposition in this part of the Faroe Shetland basin has the same provenance as that in

Kangerlussuaq. The evidence from white mica age populations corroborates conclusions based on foral

provenance and indicates similar provenance for both arenaceous and argillaceous sediments. Further, the

dominant caledonian peak in all samples (mode around 425Ma) indicates that the origin of the micas was not

Kangerlussuaq which lies west of the caledonian front and was not affected by the caledonian orogeny. Micas

eroded from basement rocks in Kangerlussuaq yield proterozoic detrital micas and yet most detrital mica

samples from Cretaceous sediments in Kangelussuaq and the Faroe Shetland basin yield dominantly

caledonian ages. Micas and pollen and spores behave similarly in water and may thus have travelled similar

distances,much further than heavy minerals. This may indicate ultimate sources in the caledonian mountains

to the east,or in reworked caledonian molasse hidden beneath the ice.

recycling of arboniferous sediments from rift

flanks

An earlier study focussed on Paleogene sediments in Kangerlussuaq but with some Cretaceous sediments,

showed strong variations in similar aged sediments. Figure 26c shows Cenomanian/Turonian sediments from

the previous study with an identical pattern to that seen in the present work. Figure 26b shows a probablility

distribution plot for Campanian/Maastrictian sediments and a remarkable lack of Proterozoic micas. Figure

26a shows the age distribution in Paleogene sediments which show a pattern similar to the

Cenomanian/Turonian pattern.

White micas separated from sediments of the Ben Nevis area of the Faroe Shetland basin (ditch cuttings from

219/21-1) exhibit a very different and anomalous age pattern. In contrast to all other samples analysed from

the Faroe Shetland basin and Kangerlussuaq, this suite of samples yielded no caledonian micas (circa 400-

450Ma). These samples yielded a narrow range of ages 894-980Ma, with a mode at 930 Ma (Figure 27a) and

similar age range within each sample (Figure 27b). In addition to the anomalous age structure the white micas

in this sampale suite were generally large (up to 1mm diameter, unaltered and undeformed) compared with

Kangerlussuaq (generally less than 500 microns diameter, sometimes showing signs of peripheral alteration,

and deformed). We investigated drilling muds used during the process in this particular well and discovered

that mica had been used as a component of a ‘Millica’ loss circulation material during the drilling, but we have

not been able to acquire a sample to test, and we are pursuing this issue. The micas extracted and measured

from well 219/21-1are likely to be a contamination and do not yield geological information. In order to

investigate what Ben Nevis well might have yielded we refer to Cretaceous samples from the basin analysed in

a previous Open University study. See table below,

37

0 500 1000 1500 2000 2500

Age (Ma)

Rela

tive

pro

bab

ilit

y

0 500 1000 1500 2000 2500

Age (Ma)

Rela

tive

pro

bab

ilit

y

0 500 1000 1500 2000 2500

Age (Ma)

Rela

tive

pro

bab

ilit

y

(a) Paleogene sediments

(b)

Campanian/Maastrictian

sediments.

(c) Cenomanian/Turonian

sediments

38

850 870 890 910 930 950 970 990

Age (Ma)

Rela

tive

pro

bab

ilit

y

0 500 1000 1500 2000 2500

Rela

tive

pro

bab

ilit

y

Figure 27. Probability plots of white micas extracted from ditch cuttings from well 219/21-1 in the Ben

Nevis area. The age range for individual samples is similar to the variation of the entire suite indicating no

variation between samples within the suite.

(a) Whole sample suite

(b) Individual samples

plotted separately

39

0 500 1000 1500 2000 2500

Age (Ma)

Rela

tive

pro

bab

ilit

y

0 500 1000 1500 2000 2500

Age (Ma)

Rela

tive

pro

bab

ilit

y

0 500 1000 1500 2000 2500

Age (Ma)

Rela

tive

pro

bab

ilit

y

Figure 28.Three probability plots from the Faroe Shetland basin. Although the number of samples from

Cenomanian/Turonian and Campanian/Maastrictian sediments are limited, the pattern is clearly identical

to that seen in Kangerlussuaq (Figure 26).

40

CONCLUSIONS

A Norwegian flora

A Greenland flora

A Scottish flora,

Within the Campanian Maastrichtian palynofloras recovered in this study,there are three major types which

represent different source vegetation (Figure 29).These can be defined using multivariate statistics, but are

also evident from empirical inspection of the data set.They comprise:

, which is highly diverse and contains similarities to palynofloras recorded from other

Northern European sites (Chalnova et al.,1981).Characteristic of this is the combination of triprojectate and

Normapolles group pollen with pollen of laurel types.

, which contains a moderately diverse triprojectate assemblage, and has a moderately

diverse suite of bryophyte spores. Younger parts of the interval show an increasing dominance of

species.This indicates that the origins of the Paleocene Greenland flora (Jolley et al.,2005)

are within the Campanian.

Within Greenland,our data indicates that west Greenland was wetter than the eastern side.

which is characterised by an abundant and diverse triprojectate flora.The remainder of the

assemblage is composed of bryophyte spores, fern spores and gymnosperm pollen, and is not highly diverse.

Despite being further to the south, it lacks the thermophyllic laurel and Normapolles elements of the

Greenland flora. This may reflect isolation and endemic floral community evolution during the Late

Cretaceous. Other records of this flora are scarce, but it is recorded as reworking in the sub-basaltic basal

Paleogene sediments of Mull (Simpson,1962, Jolley et al.,2002)

Data for the older Turonian-Santonian interval is less equivocal, but indicates that the Campanian

Maastrichtian argillaceous sediment transfer model applies here also. Because of the similarity to the later

period in the terms of mudstone deposition in a marine basin during a period of high relative sea level, this

conclusion is intuitive. It is not possible to demonstrate the presence of a distinctive Norwegian flora during

this period,because sediments of this age from offshore Norway have not been examined.

Analysis of the pollen and spore flora suggests that major changes in composition occur in response to

climatic variation.Significant cooling is demonstrated to have occurred in terrestrial environments at the end

of the Santonian,with subsequent warming occurring in the upper Campanian.This provides a stratigraphy for

pollen and spore assemblages in the region, although currently it does not compare with the resolution

available from other micropaleontological data.

By combining this study with that reported by Jolley et al., (2005) and Jolley & Morton (2007), a complete

phytogeography and argillaceous sediment transport history can be developed for theTuronian to Paleocene

(to top Sequence T38) can be utilised.

In the region of the Faroe Islands a sediment bypass system developed in Santonian - Early Campanian (Larsen

et al., 2005).The new data gathered here indicates that westerly sediment transfer into the Faroe-Shetland

Basin dominated the Late Cretaceous period. Although the lack of borehole coverage means that direct

evidence is not available, sequences of Cenomanian - Coniacian and Late Campanian - Maastrichtian

mudrocks could be expected to occur under the Faroe Islands.There remains the possibility that westerly

sourced clastic sediments of Santonian - early Campanian age may occur in this area.These are more likely to

host arenaceous beds by virtue of them being deposited during a period of low relative sea levels.

Detrital mica age evidence indicates similar sediment pathways as palynological evidence and a Greenland

sediment source in the Faroe-Shetland Basin. However, the ultimate source of silicate grains in argillaceous

and arenaceous sediments must have been dominated by the Caledonian fold belt,or sediments derived from

these rocks (e.g.Carboniferous, Jurassic).


41

Voring

Plateau

Kangerlussuaq

North Sea Basin

Faroe Islands

Faroe -Shetland

Basin

Hold with Hope

Greenland flora

Norway flora

Scotland flora

Figure 29: Map showing reconstructed argillaceous sediment supply pathways during the Campanian -

Maastrichtian. Evidence suggests that a similar pattern of sediment distribution occurred during the older,

Turonian - Santonian interval in the region between Kangerlussuaq and the Shetland Islands.

KEY

42

43

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