221
Palaeogene benthic foraminiferal biostratigraphy of the Hallen Terrace area, Norway
SUSAN KINSEY GEOMAR, Wischhofstr. 1-3, Gebaude 4, 24148 Kiel, Germany. Carrent address: Earthkind, Town Quay, Poole, Dorset, BH15 1Hj, U.K.
ABSTRACT Benthic foraminiferal assemblages were studied from four wells on the Norwegian Shelf near the Halten Terrace. A biostratigraphic scheme based mainly on benthic foraminifers but also including planktic foraminifers, diatoms and radiolarians is proposed for the Palaeogene interval which enables the correlation of the four wells. The scheme has been correlated to other biostratigraphies from the same or adjacent areas such as the North Sea and Barents Sea. The late Palaeocene is characterised by abundant and diverse agglutinated foraminiferal assemblages. The Palaeocene/Eocene boundary marks the opening of the Norwegian-Greenland Sea and a change to more impoverished assemblages. Above this there is a brief interval where planktic foraminifers are recorded, before a return to wholly agglutinated, organically cemented assemblages. Biosiliceous sedimentation and deteriorating oxygenation started in the Eocene, and continued throughout Oligocene and early Miocene.
INTRODUCTION history (Myhre et al., 1992; Thiede & Myhre 1996b). Several attempts have been made to produce a The whole region has undergone several rifting foraminiferal zonal scheme for the area of the phases throughout its history and has been a Norwegian Sea (Hulsbos et a/., 1989; Osterman & depositional centre since the Carboniferous Qvale, 1989; Kaminski et al., 1990; Poole & Vorren, (Eldholm et al., 1989). After the Caledonian 1993; Gradstein & Backstrom, 1996; Osterman & orogeny there was a period of subsidence and sedi Spiegler, 1996; Nagy et al., 1997). The main problem mentation, while later Palaeozoic tectonism encountered when trying to correlate schemes from resulted in a series of rotated fault blocks filled in the Norwegian Sea to other areas such as the North with sediment. During the late Palaeozoic-early Sea, Labrador Sea and Northern Atlantic is that for Mesozoic a general smoothing of relief took place much of its history the Norwegian-Greenland Sea forming a large regional basin iri"the early Jurassic. has been an isolated basin with hydrographic prop Much of the later Palaeozoic sedimentation has now erties often very different from those of the main been lost through later Mesozoic uplift and erosion North Atlantic. This, coupled with its high lati (Eldholm et al., 1989). tude position, has led to relatively low diversity During the Jurassic and Cretaceous the area foraminiferal assemblages, including slowly evolv underwent a period of extensional tectonism which ing, endemic species which cannot be easily com caused widespread crustal thinning and rifting. The pared to other coeval assemblages from the related culmination of these events led to most of the present areas of the North Sea or Labrador Sea. However, series of basins and highs observed today. As a such studies have proved of use in deducing and consequence of this crustal thinning and rifting there unravelling the palaeoceanographic and tectonic was an upwelling of deep mantle material in the history of the Norwegian Greenland Sea and are area which subsequently, due to cooling, led to fur especially useful in determining the histories of the ther subsidence (Boen et al., 1984; Eldholm et al., submergence of the Greenland-Scotland (Iceland 1989). Tertiary movements of plate boundaries Faroe) Ridge and of the connection to the Arctic through the Norwegian-Greenland Sea were pre Ocean through the opening of the Fram Strait. ceded by renewed lithospheric extension in the late Cretaceous and/or early Palaeocene (Myhre et al., STUDY AREA 1992). The locations of the four wells: 6406/8-1, 6406/11-s, The M0re-Trondelag shelf from about 62°N to 6407/7-2, 6407/9-3 on the Norwegian Shelf are 65°N, shows large variations in depth and width shown in Figure 1. Present day water depths of the and has a relatively steep slope cut by submarine wells range from 279 m to 348 m. troughs and channels. The southern area in general The present day Norwegian Shelf margin is a has depths of less than 200 m and is narrow with Cenozoic feature but much of its post-depositional widths of 60-80 km. Further to the north the shelf history was determined by its pre-opening structural expands to widths of up to 180-200 km and is also
In: Hart, M.B., Kaminski, M.A., & Smart, C.W. (eds) 2000. Proceedings of the Fifth International Workshop on Agglutinated Foraminifera. Grzybowski FOllndation Special Pllblication, 7, 221-241. 222 Susan Kinsey
o 20 40 60 80 100km
Figure 1. Location of the studied wells on the Halten Terrace. ESC - escarpment; FZ - fracture zone; FC - fault complex; B basin complex; H - high; PL - platform; TR - trough; SP - spur; depth contours in metres. Modified from Hammar & Hjelle (1984).
deeper than its southern counterpart, generally around the time of the Palaeocene/Eocene boundary having depths greater than 200 m. Large depressions at about 57.5 Ma (Eldholm et aI., 1989; Talwani & and channels of up to 540 m are also found Eldholm, 1977). Between Anomalies 25/24B and 13 (Holtedahl, 1993). The nearby Fwya Bank and Greenland moved in a NW direction relative to Halten Bank are extensive and have minimum Eurasia. At about the time of Anomaly 13 the pole of depths of 100-150 m (Holtedahl, 1993). The More rotation changed and the relative plate motion Trondelag and Kristiansund-Bodo fault complexes changed to west-northwest. This change in the rela plus a number of major structural highs also occur in tive spreading direction is associated with the ces this area (Hamer & Hjelle, 1984). sation of spreading in the Labrador Sea and the Prior to the opening of the Norwegian Sea, the change in the plate geometry, with Greenland continental part of the present margin may have becoming part of the North American Plate. This in been either a shallow epicontinental (Myhre et ai., turn led to the opening of the northern Greenland 1992), or mid- to upper bathyal (Gradstein, pers. Sea (Eldholm et ai., 1989; Myhre et ai., 1992). comm., 1998) sea which extended into the North Sea During the Palaeogene, deposition along the and Barents Sea. During the early Tertiary the rifted margin was dominated by rift induced uplift opening of the Norwegian-Greenland Sea occurred which gave rise to the erosion of highs and redepo- Palaeogene benthic foraminifera of the Halten Terrace, Norway 223 sition on the outer More and Voring Basins. e.g., different modes and degrees of preservation of Continued subsidence but waning siliclastic sedimen the predominant fauna, and obviously out of place tation during the Eocene and Oligocene led to forms such as Pliocene planktic foraminifers and pelagic sedimentation becoming more important, calcareous benthic foraminifers in the predomi although the highs continued to influence sedimen nantly agglutinated sections of the Palaeocene and tation until their burial in the late Oligocene Eocene. Samples from the wells were studied (Myhre et al., 1992). Later erosion has meant that on approximately every 10-20 m. Sampling usually the northern part of the shelf only thin Eocene began at about 100-300 m below the sea floor. Above sequences are seen, while Oligocene sediments are this, sample material was not collected but returned only preserved on Halten Bank (Stuevold & straight to the sea bed. Eldholm, 1996). Since the amount of sample received for each The Fram Strait provides the sole passage well varied widely (e.g., from 5-50 g) and from each between waters of the Arctic and the Norwegian sample a micropalaeontological, sedimentological Greenland Sea. Although it was probably open as a and archive split needed to be taken, it was not pos shallow passageway from the late Oligocene, it was sible to take the same amount of sample from each probably not until the mid-Miocene that it reached well or depth. Where enough material was avail sufficient depth (around 2 km) to allow deeper able, a subsample of 20 g or greater was taken for waters from the Arctic into the Norwegian Sea micropalaeontological purposes. In the case of Well (Kristoffersen, 1990). 6406/8-1 much less material was available and Up until the early mid-Miocene it seems likely therefore the samples were often 10 g or less. that very little or no abyssal water exchange took The samples were first soaked in distilled water place into the main North Atlantic - the Greenland for 24 hrs, freeze-dried and then weighed to obtain Scotland Ridge acting as a barrier to deep water the total dry weight of sediment. Due to the high exchange. However, eastern parts of the ridge, i.e., clay content, which proved difficult to get rid of the Faeroe-Shetland Channel may have been below especially in the lower samples, a number of further sea level during the Eocene to at least bathyal preparation methods were tested to disaggregate depths as similar benthic foraminiferal assem the clay. blages have been reported from both the Norwegian The most successful method in terms of both time and Labrador Seas (Kaminski et al., 1990). Eocene and efficiency and the one that was finally bottom waters were probably relatively warm with adopted, was to first soak the samples in dilute little current activity taking place (Miller & hydrogen peroxide (1 part 35% H 20 2, to 4 parts Tucholke, 1983). During the Palaeocene and Eocene water) for a maximum of 24 hrs, wet sieve through a surface water connections may have existed with 63 J.Lm sieve and then dry at 40°C, although even the North Atlantic as witnessed by the presence of with this method some clay aggregates remained. temperate to subtropical siliceous faunas and floras However, with even harsher methods of prepara recorded during ODP Leg 151 (Thiede & Myhre, tion, there was the risk that some foraminifers 1996a). Cool to temperate waters probably first would also be destroyed, so it was felt that some appeared during the late Oligocene to early Miocene compromise had to be made between efficiency of (Thiede & Myhre 1996a). clay removal and preservation of microfossils. Deep water and abyssal overflow across the The dried samples were then sieved into the frac Greenland-Scotland Ridge probably did not take tions 63-125 J.Lm, 125-250 J.Lm, 250-500 J.Lm, 500-1000 place until the mid- to late Miocene, about 13-11 Ma. J.Lm and >1000 J.Lm and weighed. For the micro and occurred first across the Iceland-Scotland seg palaeontological investigations the fractions 125- ment of the ridge (Bohrmann et al., 1990). 250 J.Lm, 250-500 J.Lm and 500-1000 J.Lm were used. Using a binocular microscope foraminifers were picked from each depth and mounted on faunal METHODS AND MATERIALS slides. Wherever possible at least 300 foraminifers The analyses were carried out on cuttings samples. In were picked. Other microfossils such as ostracods, using cuttings samples there is the problem-ugh diatoms, radiolarians, bolboforma, and fish teeth 'caving', i.e., microfossils from stratigraphically were also picked and/ or counted. younger strata falling down-hole, destruction of delicate taxa and size sorting. For a full account of BIOSTRATIGRAPHY the problems inherent in using such material see The assemblages of the four wells in this study were King (1983). Therefore, the most reliable method for defined by using first downhole occurrences and acme constructing a biostratigraphic time scale or occurrences of benthic foraminifers - both aggluti zonation scheme is by recording the extinctions (or nated and calcareous. Within each well the extinc first down-hole occurrences) of species, using tions or last occurrence (LO) and last common relative abundances of taxa and acme occurrences as occurrence (LCO) of microfossils were noted. these are less affected by such problems and more Figure 2 shows the assemblages defined for each likely to be in situ. Obviously out of place of the wells. Using the observations from the four foraminifers can be recognised by a variety of means, wells a composite biostratigraphy was created. 224 Susan Kinsey
CII . "' s § ~ ~. t l s" Ii.• § 1 j 9 til . i I. II·u ! ~: •• i :Ii •t it \~ 1 J "'CII i il CII l~ HI; i !~ U j It H ::':~uj~ j~ j < ... ~
I/) UJ I~g ~ s ~ .~ < i~i i ~. L "..J ~i[ s E~ OJ Bq 1 ~ l H ~ ~l :Ii HH ~i'." ~ ! i H i it ~l ~ ! ~ ~ I! CII i .~ '" d~l~ ~ ¢ - ~cc U~~ Ii ~ ..... ~~~ ~ 1
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! .~ ~ j \ i 1 J q ·ll iii ~! ttl .!, I ~ 1 i i I it j II! "' Ai !q i 1 1 i ~ t t ~~~ "' f!" t i ~ j"~ '" JM j ] I ~ ~i i-W it 'f i'¥ t W g (W)I4I~ 2 ~ ii ~ ~ ~ ~ ~ ~ ~ 2 ~ ~ ~ ~ ~ ~ II) i "'a: ~ Ii ~ • i ~! ~ i I &1 n~ E", .l!wd ..II) ~~ ·i~ ~.~ .3 U Hi II
CII ~ ~ ~ I ~ t '" I .s ~ ~ s" § ! t ~ til i I j! t ~ :Ii ~ I ~I ~ ~ ~ UJ 11 i .3 iii E en f i H ! iI <"' i ! It ~ i!it ~ H j ~ I 1 I I I § ~ ~ f
Figure 2. Microfossil assemblages and first & last occurrences in each of the Halten Terrace wells studied. Palaeogene benthic foraminifera of the Halten Terrace, Norway 225
Although the emphasis of this work is upon benthic 2. Impoverished Assemblage foraminifers, in some intervals these are either not Age: late Palaeocene/ early Eocene present or are not age diagnostic. Thus, in order to Low abundance and low diversity assemblage with present a stratigraphic scheme that is as complete foraminifers similar to those from Assemblage 1. as possible and contains easily identifiable and, where possible, abundant markers, other groups, 3. Coseinodisells spp. Assemblage namely planktic foraminifers, diatoms, bolboforma, Age: earliest Eocene and radiolarians, were also incorporated into the Generally low diversity and abundance assemblage biostratigraphy. Such an integrated approach is characterised by the appearance of large numbers of useful when dealing with cuttings samples which pill box shaped diatoms assigned to CoscinodiscliS may often be small in quantity and variable in qual spp. These are generally pyritized. The ity and has been successfully applied by Gradstein foraminifers that are seen are again those from et al. (1994) and Gradstein & Backstrom (1996) to Assemblage 1. the Halten Bank and North Sea areas. Dating the samples was further complicated by the general 4. Subbotina patagoniea Assemblage lack of index planktic foraminifers and of isotopic or Age: early Eocene magnetostratigraphic data. The assemblage is characterised by an influx of the planktic foraminifer S. patagonica. These often PROPOSED BIOSTRATIGRAPHIC SCHEME FOR have a pink colour. There is also a return to high THE HALTEN TERRACE AREA agglutinated benthic diversity and abundance. Figure 3 shows the assemblages of the composite bio Many of the foraminifers recorded are again similar stratigraphy and their characteristic microfossils. to assemblage I, although ammodiscids decrease in Lower Palaeocene and Upper Eocene sediments were importance. Reticlilophragmium intermedia and not observed in the wells studied. This is common in Buzasina galeata are generally confined to this the Norwegian Sea and especially so on Halten assemblage. The benthic foraminifers are again Bank (Dalland et al., 1988; Kaminski et al., 1990; finely grained. In contrast to assemblage 1 the il'stS Myhre et al., 1992; Gradstein et al., 1994; Gradstein are usually white to cream in colour. & Backstrom, 1996; Stuevold & Eldholm, 1996). The Lower Palaeocene hiatus has been ascribed to Late 5. Karrerulina spp. - Spiroplectammina navarro ana Cretaceous/Palaeocene syn-rift uplift (Stuevold & Assemblage Eldholm, 1996) and the upper Eocene hiatus to Age: early Eocene intensified deep sea circulation leading to erosion Again an abundant and diverse assemblage with (Thiede et al., 1989; Tucholke & Mountain, 1986). acmes in the nominate taxa. Haplophragmoides The top of the mid-Eocene here is marked by a loss kirki and H. porrectus are also important. of foraminifers and a large increase in siliceous Reticulophragmium amplectens also appears in the microfossils. The absence of the early Palaeocene assemblage but has its acme in the overlying one. and late Eocene index fossils (as defined by Gradstein et al., (1994) and Gradstein & Backstrom 6. Retieulophragmium ampleetens Assemblage (1996)) further points to the absence of these Age: mid-Eocene sediments in the wells studied although bad Diversity tends to decrease within this assemblage preservation and very low numbers of foraminifers as R. amplectens is very dominant, often more so recovered from the Middle Eocene onwards make than the tubular forms. Other typical foraminifers exact identification and division of zones somewhat include Cribrostomoides sp. Recurvoides spp. difficult. In general, tubular forms such as Budashevaella multicamerata and Ammomar Rhabdammina spp., Rhizammina spp. and ginulina aubertae. Siliceous microfossils, mainly Bathysiphon spp. dominate all the assemblages. radiolarians, also start to appear within this Figure 4 shows the correlation of the four wells with assemblage in large numbers. one another. 7. Glomospira eharoides Assemblage 1. Troehammina ruthvenmurrayi - Age: late mid-Eocene Spiropleetammina speetabilis Assemblage Abundance and diversity decrease further within Age: late Palaeocene this assemblage. The foraminifers also tend to be Diverse and abundant assemblage which is exclu less finely finished and slightly coarser grained. sively composed of agglutinated foraminifers. The The most noticeable feature of the assemblage is the foraminifers have finely grained and smoothly fin small influx of the nominate taxa. Siliceous micro ished tests - often green or brown in colour. The top of fossils are again dominant. the assemblage is marked by the LCO of S. spectabilis. In general the foraminifers are typical 8. Turrilina alsatiea - Spirosigmoilinella eompressa 'flysch-type' faunas. Rzehakina minima, Assemblage Subreoplwx spp. and Troehamminoides spp. are gen Age: early Oligocene/?late Oligocene erally confined to the assemblage. A low abundance and diversity assemblage. 226 Susan Kinsey
Assemblages
EMio.
Unzoned ------Interval L. Olig. Characteristic microfossils
Occasional calcareous benthics 9 ------radiolarians, diatoms Turrilina a/satica Turri/ina alsatica Spirosigmoilinella compressa 8 E.Olig. Coarse agglutinated foraminifers
Glomospira charoides Cyclammina placenta 7
L.Eo. Reticulophragmium amplectens Cribrostomoides spp. Recurvoides spp. 6 Haplophragmoides spp.
Karreriella conversa Karreriella horrida AmmomarginuJina aubertae Reticu/ophragmium Spiroplectammina navarroana M.Eo. Reticulophragmium amplectens 5 amp/ectens Haplophragmoides kirki Haplophragmoides porrectus Recurvoides spp. Subbotina patagonica Karreriella con versa Karreriella spp. Karreriella horrida 4 Spirop/ectammina navarroana AmmomarginuJina aubertae Spiroplectammina navarroana Subbotina patagonica E.Eo. Reticulophragmium intermedla Coscinodiscus spp. Coscinodiscus spp. foraminifers from Assemblage 1 3 - -ImpOVeriShed ------Trochammina ruthvenmurrayi Scattered appearence of foraminifers from Assembla e 1 2 L.Pal. Trochammina ruthvenmurrayi Spiroplectammina spectabilis Saccammina placenta Trochamminoides spp. Ammodiscus spp. 1 E. Pal. Glomospira spp. Haplophragmoides walteri Bathysiphon spp. Rhabdammina spp.
Figure 3. Microfossil assemblages and characteristic taxa for the proposed Halten Terrace biostratigraphy Palaeogene benthic foraminifera of the Halten Terrace, Norway
279m Sea floor 315m ~ _~~~m~ ____-- __------______338m~ ~ __~
640719-3
rnIej,MIo,
6I.07n-2
6406111 -1
10 ~ MaIIInoItIoIIo COfM!UI!io • 8oIbcI0ImlI _ .
8 G Unzoned iI'IIerva'
8~ T""'N ...., " . ~_
7 m GJomooph charoJdo.
6 0 R.,ic1J/opIngmJom 0Irp/«I.".
Figure 4. Correlation of the Halten Terrace wells, based on microfossil last occurrences. 228 Susan Kinsey
Apart from the two nominate taxa Rotaliatina are often only local due to hiatuses, changing envi blilimoides is also occasionally recorded. Coarse ronmental conditions etc. whereas the optimum agglutinated foraminifers and some poorly sequence, which is the composite result of many preserved calcareous benthics may also be present. wells, minimises these effects. Siliceous microfossils again dominate. The work of Nagy et al. (1997), based on wells to the north of this area, has results similar to those in 9. Unzoned interval this study. They also report a low diversity section Age: ?late Oligocene/early Miocene around the Palaeocene/Eocene boundary and their Extremely poor assemblages. There may also be bar Early Eocene assemblages contain high abundances ren sections. A few badly preserved calcareous of Spiropleetammina navarroana and Karrerlliina foraminifers may be observed. Siliceous microfossils, spp. However, they did not observe the influx of especially radiolarians, are dominant. Subbotilla patagollica and speculated that this was either due to the northern boundary of the species COMPARISON WITH OTHER being south of the Barents Sea or that the bottom BIOSTRATIGRAPHIC SCHEMES waters were too corrosive for calcareous microfossils The biostratigraphy here has been correlated with to be preserved. other schemes from the same or adjacent areas. The ODP Site 643 on the slope of the V0ring Plateau main schemes published to date are discussed below. (present day water depth 2768 m) was much deeper Figure 5 shows the approximate correlation between than the sites studied here. Kaminski et al. (1990) the biostratigraphy from this study and those most reported that the site was at mid-bathyal depths in relevant to it. the early Eocene, lower bathyal depths in the mid Gradstein et al. (1992), Gradstein et al. (1994) Eocene and by the Early Oligocene was abyssal. The and Gradstein & Backstrom (1996) have produced sites on the Halten Terrace, however, underwent a composite biostratigraphies for the northern North shallowing through time. One of the main differ Sea area and Halten Bank incorporating both ences to be noted is in the Retielliophragmium foraminifers and dinoflagellates. Their material ampleetells range. At ODP Site 643 it ranges into the also consisted of cuttings. To produce the biostrati upper Oligocene while in the Halten Terrace area graphy they used two quantitative biostratigraphy its LO is within the upper mid-Eocene. If R. software programs: 1. Ranking and scaling which ampleetells is a 'deep' water species then this may considers the stratigraphic order of all (pairs of) be the explanation for its earlier disappearance on events in wells simultaneously and calculates the the Halten Terrace. Kaminski et al. (1990) also most likely sequence of events (Gradstein & stated that their Glomospira spp. Assemblage rep Backstrom, 1996); and 2. a probabilistic graphic resents the first appearance of Glomospira into the zonation using the program STRATCOR. For fuller Norwegian Sea. Karrerulilla eOllversa and details on how these programs work see references Troehamminoides sp. also all had first occurrences in cited above. this assemblage during the early middle Eocene. The LO sequences observed in each well in this However in the Halten Terrace wells all these study were correlated with this optimum sequence. forms are also present in the Palaeocene and the In general, the plots show a good correlation apart Glomospira assemblage would seem to occur some from the LO of Saeeammina placenta and the LO of what later, in the late mid-Eocene. Kaminski et al. Spiropleetammina speetabilis which plot consis (1990) also found the ranges of Spirosigmoilillel/a tently higher in the Halten Terrace wells. In both eompressa and Retieulophragmium ampleetells over cases in the wells studied here, above the lapping is not observed in any of the wells studied Palaeocene their appearance is very sporadic and here. In general many of the agglutinated they are generally not well preserved. This may foraminifers observed in ODP Site 643 seem to range indicate that they have been reworked which much higher - up into the Miocene - than those from would account for the differences seen. Those the Halten Bank area. It has also been noted in the microfossil events that plot lower (e.g., the LOs of Palaeogene of the Labrador Sea and Labrador Cyc/all1mina rotundidorsata and Adereotryma 'Shelf' (Kaminski et al., 1989a; Gradstein et al. agterbergi in wells 6407/7-2,640678-1 and 6407/9-3) 1994) that agglutinated foraminifers disappear may be due to only partial ranges being observed in much earlier - around the Eocene/ Oligocene the Halten Terrace wells and to caving. Gradstein & boundary. The later disappearance of agglutinated Backstrom (1996) also noted that in their Halten foraminifers in the deep sites of the V0ring Slope is Bank wells the LO of Karrerulina con versa occurred probably due to the waters of the Norwegian Sea within the Upper Palaeocene. However in the wells remaining stratified throughout the Palaeogene and studied here the LO of K. con versa is found within early Neogene with deeper waters being more the mid-Eocene and therefore corresponds well with corrosive (Kaminski et al., 1990). their final optimum sequence. Osterman & Spiegler's (1996) zonation for Site The differences between the optimum sequence 913 in the Greenland basin is similar to those for the and the order of LOs between individual wells are Halten Terrace, in that their Eocene assemblages mainly due to the fact that within each wells LOs were predominantly agglutinated and dominated by Palaeogene benthic foraminifera of the Halten Terrace, Norway 229
Gradsteln & Nagy et al. 1997 Backstrom '96 Poole &Vorren '93 Kaminski et al.'90 King 1989 This study
NSB5 NSR5B Ammomarginu/ina R. amp/eetens aubertae NSA5 G/omospira spp. NSR5A
NSA4 NSB4 Karreriella spp. S. navarroana Retieu/ophragmium amp/eetens NSB3 E.Eo. I------i spp. NSB2
NSAl Troehammina ruthvenmurrayi
~Hiatus W~ H'laluses common ~I Not studied
Figure 5. Approximate correlation of Halten Terrace biostratigraphy to other biostratigraphic schemes. 230 Susan Kinsey
Reticuiophragmium ampiectens. These authors also relatively nutrient rich, warm waters. Deposition found that middle-late Eocene to Oligocene assem was below the CCD as witnessed by the absence of blages showed a drop in diversity and abundance. calcareous benthics or planktics. Tubular forms, e.g., However, their most interesting result was that Rhabdammina and Bathysiphon are dominant. many of the foraminifers from Site 909 in the Fram Ammodiscids, haplophragmoidids and Karreruiina Strait ranged into much younger strata than else spp. are also common. where. Reticuiophragmium ampiectells for example 2. Impoverished/barren intervals at or near the had its LO in Miocene sediments. Normally, this Palaeocene/Eocene boundary. These probably relate species has its acme occurrence in the mid-Eocene to the opening of the Norwegian-Greenland Sea. and its highest LO was reported by Kaminski et ai., Pyritized diatoms are common at the top of the (1990) to be in the Late Oligocene. Osterman & interval. There was subsequently an interval of Spiegler (1996) postulated that a deep-water basin increased current activity together with some uplift in the Fram Strait area was responsible for the and a deepening of the CCD. Assemblages containing anomalously long ranges of the foraminifers from the planktic foraminifer Subbotina patagonica are Site 909 and that this basin remained isolated from common during this interval. The appearance of the rest of the North Atlantic until the Miocene. subbotinids during the earliest Eocene indicates a During Phase 1 of this project (Steurbaut et ai., position above the CCD, they may also imply a 1991), wells from the northern North Sea were also cooling of at least the surface waters as subbotinids studied and samples were investigated from the are thought to be cool water indicators (Pardo et ai., whole of the Cenozoic. A pattern of agglutinated 1997). assemblages with large numbers of Rhabdammina 3. Purely organically cemented agglutinated assem like tubes in the Palaeocene and mid- to late Eocene blages are found in the lower Eocene. Tubular forms (late mid-Ypresian to late Rupelian) was observed. increase in abundance and the rest of the fauna (e.g., During the early Eocene (early to mid-Ypresian) Karreruiina conversa, Recurvoides spp.) together assemblages with high numbers of planktic with reduced numbers of ammodiscids and lower foraminifers were recorded. As in this study the TOC values indicate relatively deep, quiescent, agglutinated assemblages disappeared within the waters and a return to more oxygenated conditions upper middle Eocene to Lower Oligocene section. In below the CCD. contrast to this work they found planktic-rich 4. The mid-Eocene heralds the start of siliceous assemblages in the lower part of the upper sedimentation, increased organic matter Palaeocene, and abundant and diverse calcareous accumulation and a deterioration of subsurface benthic assemblages from the lower Oligocene oxygen conditions. Assemblages are dominated by onwards. Reticuiophragmium ampiectens. Enhanced surface King's (1989) zonal scheme for the North Sea can productivity increased nutrient flux to the sea floor also be applied to some extent within the leading to more eutrophic conditions. The decrease Norwegian shelf area. As can be seen from the in diversity of agglutinated foraminifers towards assemblages devised for the Halten Terrace area the top of this interval may also point to shallower there are very few calcareous benthics to be found in conditions. In the upper Middle Eocene the Palaeogene and Lower Neogene so during this impoverished foraminiferal assemblages, often time only the NSA zones are applicable. with Glomospira charoides, are recorded. Siliceous Kaminski et ai. (1989a) noted that in the microfossils, especially radiolaria, dominate. Labrador Sea at ODP Site 647 the Palaeogene 5. During the Oligocene and early Miocene there was assemblages are predominantly agglutinated and a domination by siliceous microfossils. Numerous that there is a turnover of benthic foraminifers hiatuses and barren periods indicate an increase in around the Eocene/Oligocene boundary from current activity. The very high numbers of predominantly agglutinated assemblages to poor radiolarians recorded may point to waters deeper calcareous ones. This is similar to the findings from than 150m, (Hull, 1996). Foraminiferal assemblages the Halten Terrace, although the assemblages at are impoverished with either mainly agglutinated the Halten Terrace seem to remain poor for much (Oligocene) or calcareous (Miocene) foraminifers. longer than those in the Labrador Sea. The change The appearance of calcareous foraminifers indicates in assemblages at the Eocene/Oligocene boundary deepening of the CCD and/or shallowing of the was related to changes in the preservation of sites. The presence of Turrilina aisatica may indi agglutinated species and to the first appearance of cate low to intermediate bottom water oxygen cool, nutrient poor, deep water into the southern conditions (Kaiho, 1991). Labrador Sea (Kaminski et ai. 1989a). SUMMARY PALAEOENVIRONMENT 1. A total of nine assemblage zones for the Using changes in the foraminiferal assemblages five Palaeogene were identified using a combination of main changes in palaeoenvironment can be defined. foraminifers (agglutinated and calcareous) and 1. During the late Palaeocene the sites studied other microfossils such as diatoms and radiolaria. probably experienced deep water conditions with The biostratigraphy created has been correlated Palaeogene benthic foraminifera of the Ralten Terrace, Norway 231 with other schemes from the same or adjacent areas. impoverished agglutinated assemblages that were Biostratigraphical schemes from the Norwegian dominated by silicious microfossils. The Oligocene Sea were found to be most similar, while those from and early Miocene were times of increased current the North Sea, although applicable in many activity, high biosilicious input and falling sea respects, could not be used if based upon planktic levels. Assemblages are extremely impoverished to foraminifers. Calcareous benthic zonations could barren, although the beginning of improved condi also not be used in the Halten Terrace area for the tions is seen in the Miocene with the first Palaeogene and Lower Neogene. The last observed appearance of calcareous benthics. occurrences in each well were correlated against an optimum extinction sequence for the North Sea and TAXONOMY Halten Bank area. Although some outliers were The generic classifica tion follows largely the observed the two schemes were found to be in good scheme of Loeblich & Tappan (1987). Where appro general agreement. priate, emendations from Jones (1994), Gradstein & 2. The Lower Palaeogene samples (Upper Kaminski (1989) and Kaminski et al. (1993) were Palaeocene to mid-Eocene) are dominated by used. Taxa are presented alphabetically. Only the agglutinated foraminifers. Seven assemblage zones most frequent taxa are mentioned below. The follow were identified of which five were characterised by ing abbreviations have been used: d. for taxa simi agglutinated foraminifers, one by planktic lar to the named species but differing in some detail, foraminifers and one by diatoms. ex. gr. for the sake of an example, sp. 1, 2 etc. for 3. In the Upper Oligocene to Middle Miocene species which do not match published descriptions, foraminifers (agglutinated and calcareous) can only sp. spp. for taxa not identified to specific level. rarely be used for biostratigraphic purposes. Siliceous microfossils (diatoms and radiolaria) Adercotryma agterbergi Gradstein & Kaminski, dominate. It is possible to utilise their presence in 1989 this interval together with the appearance of rare Plate 4, Fig. 1 foraminifers for biostratigraphic purposes. One zone Adercotryma agterbergi Gr~dstein & Kaminski. - Kaminski was identified which was characterised by the et ai., 1990, p. 367, pI. 4, fig. Sa-b. presence of a few planktic foraminifers together Adercotryma agterbe;gi Gradstein & .Kaminski. - Gradstein with siliceous microfossils. The section from the et al., 1994, pI. 7, fIgs 12-14. pI. 8, fIgs 1-5. Upper Oligocene to the Lower Miocene is not charac Ammodiscus cretacetls (Reuss, 1845) terised by any foraminifers or useful microfossils and Plate 3, Fig. 1 was left unzoned. Ammodiscus eretaceus Reuss. - Labude, 1984, p. 69, pI. 1, fig. 4. Although agglutinated foraminifers can often be 7. relatively long ranging and have a high tolerance to Ammodiscus cretaceus Reuss. - Kaminski et ai., 1988, p. 213, fluctuating conditions, changes in assemblage pI. 3, fig. 7. Ammodiscus cretaceus Reuss. - Kuhnt, 1990, p. 313, pI. 1, figs composition can be helpful in inferring palaeoenvi 2-3. ronments. Using evidence from changes in AmmodisClls cretaceus Reuss. - Charnock & Jones, 1990, p. foraminiferal morpho groups and in foraminiferal 154, pI. 2, figs 1-3; pI. 14, fig. 3. Ammodiscus cretaceus Reuss. - Morlotti & Kuhnt, 1992, p. and other microfossil distribution patterns, a succes 221, pI. 1, figs 1-2. sion of palaeoenvironments on the Halten Terrace can be outlined. The foraminiferal patterns are in Ammodiscus pennyi Cushman & Jarvis, 1928 fluenced by tectonic movements, sedimentation rates, Plate 3, Fig. 3 circulation patterns and changes in organic flux. Ammodiscus pemzyi Cushf!lan & Jarvis. - Kaminski et ai., 5. During the late Palaeocene the sites studied 1988, pp. 184-185, pI. 3, figs 9-10. experienced deep water conditions below the CCO AmmodISCUS pennyi Cushman & Jarvis. - Kuhnt, 1990, p. with relatively nutrient rich, warm waters with 313, pI. 1, fig. 6. medium strength bottom currents. The opening of the Ammodiscus peruviantls Berry, 1928 Norwegian-Greenland Sea led to increased current Ammodisclls peruvian us Berry. - Kaminski et ai., 1988, p. activity together with some uplift and a deepening 185, p1.3, figs 11-12. of the CCO. The influx of subbotinids, which live at Ammodiscus peruvian us Berry. - Morlotti & Kuhnt, 1992, p. or lower than the thermocline and are generally 221, pI. 1, fig. 4. indicative of cooler waters, possibly indicate cool Ammodiscus tenuissimtls Grzybowski, 1898 surface to intermediate waters during the earliest Plate 3, Fig. 2 Eocene (Pardo et al., 1997 and references therein). The early Eocene is characterised by a return to Ammodiscus tenuissimus ~rzybowski. - Kaminski & Geroch, 1993, p. 253, pI. 5, fIgs 1-3b. deeper sub-CCO conditions with a reduced nutrient Ammodisclls tenuissimlts Grzybowski. - Kaminski et al., input. In the mid-Eocene siliceous sedimentation and 1996, pI. 1, fig. 4. increased organic matter accumulation led to more corrosive bottom waters and a decrease in subsurface Ammomarginulina aubertae Gradstein & Kaminski, oxygen conditions, which in turn probably caused the 1989 extinction of many foraminifers leaving only Plate 3, Fig. 12 232 Susan Kinsey
Ammomargilllllina allbertae Gradstein & Kaminski. - Cyclammina rotundidorsata (Hantken, 1875) Gradstein & Kaminski, 1989, p. 74, pI. 3, figs 1-8, pI. 4, figs 'i:yc/ammina (Retiwlopizragmillm) rotlllldidorsata (Hantken). 1-3, text-fig. 2. - Charnock & Jones, 1990, p. 176, pI. 7, figs 13-15; pI. 19, Ammomargmlllina allbertae Gradstein & Kaminski. - fig. 1. Charnock & Jones, 1990, p. 179, pI. 9, figs 6-8; pI. 20, fig. 7. Cyclammina rotundidorsata (Hantken). - Jones, 1994, p. 43, Ammomargillulina allbertae Gradstein & Kaminski. - pI. 37, figs 17-19. Gradstein et al., 1994, pI. 6. figs 15-22. Cl/cIammina rotllndidorsata (Hantken). - Gradstein et al., '1994, pI 6, figs 13-14. Ammosphaeroidina pseudopallciloclliata (Mjatliuk, 1966) Cystammina pauciloclliata (Brady, 1879) Ammosphaeroidina pseudopauciloclllata (Mjatliuk). - Plate 3, Figs 5, 7, 8 Kaminski et al., 1988, p. 193, p.1. 8, figs 3-5. Cystammina pallciloculata (Brady). - Schroder, 1986, p. 54, Ammosplweroidina pseudopallClloClllata (Mjatliuk). - Kuhnt, pI. 18, figs 14, 15. 1990, p. 321, pI. 5, fig. l. Cystalllmilla pallciloclliata (Brady). - Charnock & Jones, AmmosphaerOldina pseudopallci/oclllata (Mjatliuk). - 1990, pp. 168-169, pI. 5, fig. 7. Gradstein et al., 1994, pI. 3. figs 1-7. Cystaml1lllla pallciloClllata (Brady). - Jones, 1994, p. 45, pI. 41, fig. l. BathysipllOn annulatus (Andreae, 1890) Cystalllmina pallciloclliata (Brady). - Gradstein et al., 1994, pI 3, figs 8-12. Batllysiphon annulatlls (Andreae). - Kaminski et al., 1988, p. 184, pI. 1, figs 16-17. The assemblages studied may also contain specimens Bathlfslpizoll all/wlatus (Andreae). - Charnock & Jones, 1990, p."149, pI. 1, fig. 30; pI. 13, fig. 10. of Cysta1l1mil1a sveni Gradstein & Kaminski (1997), (Gradstein, pers. comm., 1997). Bigenerina sp. 1 Charnock & Jones, 1990 Plate 1, Fig. 4 Evoilltinella sp. 1 Bigelleri.na sp. 1. Charnock & Jones 1990, p. 184, pI. 9, figs Plate 2, Fig. 10 19-20, pI. 21, fig. 8. Planispiral, evolute coiling with 7 chambers in last Budashevaella mlllticamerata Voloshinova, 1961 whorl. Wall is finely grained. Chambers are almost Budashevaella mlliticamerata Voloshinova. - Kaminski et aI., triangular and sutures are depressed. 1990, p. 367, pI. 4, fig. 6a-b. Glo11lospira charoides (Jones & Parker, 1860) Bllzasina galeata (Brady, 1881) Plate 3, Figs 4, 9 Bllzasina galeata (Brady). - Charnock & Jones, 1990, p. 166, Glomospira charoides (Jones & Parker). - Kaminski et al., pI. 5, fig. 1; pI. 16, fig. l. 1988, p.185, pI. 3, figs 14-15. Bllzasina galeata (Brady). - Jones, 1994, p. 45, pI. 40, figs 19- Glomospira charoides (Jones & Parker). - King, 1989, p. 455, 23. pI. 9.1, fig.17. GTomospira clwroides (Jones & Parker). - Kuhnt, 1990, p. Conglopl1ragmimn coronatllm (Brady, 1879) 313, pI. 1, fig. 1l. Glomospira charoides (Jones & Parker). - Mariotti & Kuhnt, Plate 4, Fig. 9 1992, p. 222, pI. 1, figs 7-8. ConglophragmiIllII co~onatIll~l (Bradx). - Charnock & Jones, 1990, p. 167, pI. 5, figs 2-3, f'1. 16, fig. 2. Glomospira diffllndens (Cushman & Renz, 1946) Conglophragmium coronatllln (Brady). - Jones, 1994, p. 45, pI. 40, figs 8-12. Glomospira dilllmde/Is .(Cushman & Renz). - Kaminski et al., 1988, p. 185, pI. 3, figs 18-19. Cribrostomoides sllbgloboSllS fonna sllbgloboSliS (Cushman, 1910), emend. Jones et al., (1993) Glomospira glomerata (Grzybowski, 1898) Plate 3, Fig. 6 Cribrostomoides sllbgloboSllS forma subgloboslls (Cushman), emend. Jones et al., - Jones et aI., 1993, pp. 181-193, pI. 3, Glolllospira glomerata (Grzybowski). - Kaminski et al., 1988, figs 1-7. p. 185, pI. 3, fig. 16. Cribrostomoides subgloboSllS forma sllbgloboSllS Cushman), Glomospira glomerata (Grzybowski). - Charnock & Jones, emend. Jones et al., - Bender, 1995, p. 42, pI. 5, fig. 2. 1990, p. 156, pI. 2, fig. 11. Glomospira glomerata (Grzybowski). - Kaminski & Geroch, Cribrostomoides sp. 1 1993, p. 257, pI. 6, figs 9-12. Plate 3, Figs 10, 11 Glomospira glomerata (Grzybowski). - Kaminski et al., 1996, pI. 1, fig. 13. Small, almost spherical Cribrostomoides, very Glomospira gordialis (Jones & Parker, 1860) finely grained and finished. 4-5 chambers in last whorl. Sutures flush or only slightly depressed. Glolllospira gordialis (Jones & Parker). - Kaminski et al., 1988, p. 213, pI. 3, fig. 17. Cyclammina placenta (Reuss, 1851) Glomospira gordialis (Jones & Parker). - Kuhnt, 1990, p. 313, pI. 1, figs 9-10. Plate 2, Fig. 3 Glomospira gordia/is (Jones & Parker). - Charnock & Jones, 1990, p. 156, pI. 2, fig. 12; pI. 14, fig. 9. Cyc/ammina (Cyclammina) placenta (Reuss). - Charnock & Glomospira gordialis (Jones & Parker). - Mariotti & Kuhnt, Jones, 1990,,P. 175, pI. 7, figs 5-12, pI. 18, fig. 4. 1992, p. 222, pI. 1, fig. 9. "Cyclammina' placenta (Reuss). - Kaminski et ai., 1990, p. 369, pI. 6, fig. 2a-b. Cyclammina placenta (Reuss). - Gradstein et ai., 1994, pI 6, Glomospira irregularis (Grzybowski, 1898) fig.7-1l. Glomospira irreglliaris (Grzybowski). - Kaminski et al., 1988, p. 185, pI. 3, figs 20-21. Palaeogene benthic foraminifera of the Hallen Terrace, Norway 233
Glomospira irregularis (Grzybowski). - Kuhnt, 1990, p. 313, Waters, 1927 pI. 1, fig. 12. GTomospira irreglliaris (Grzybowski). - Charnock & Jones, Haplop!zrag~oides walteri excavatlls ~ushman & Waters. - 1990, p. 157, pI. 2, fig. 14; pI. 14, fig. 11. Kaminski et al., 1990, p. 368, pI. 5, fIg. 6a-b. Glomospira irreglilaris (Grzybowski). - Morlotti & Kuhnt, Haplophragmoides walteri excavatus Cushman & Waters. - 1992, p. 222, pI. 1, fig. 12. Gradstein et al., 1994, pI. 7, figs 6-9.
Glol1lospira serpens (Grzybowski, 1898) Haplophragmoides sp. 2 Glomospira serpens (Grzybowski). - Kaminski et al., 1988, p. Planispiral, involute with inflated chambers. 185, pI. 3, figs 22-23. Glomospira serpens (Grzybowski). - Kuhnt, 1990, p. 313, pI Sutures are flush and the wall is smooth and finely 1, fig. 4. grained Glomospira serpens (Grzybowski). - Kaminski et al., 1996, pI. 1, fig. 15. Kalamopsis grzybowskii (Dylqianka, 1923) Haplophragmoides d. concavus (Chapman, 1892) Kalamopsis grzybowskii (Dylqianka). - Kaminski et al., 1988, p. 187, pI. 1, figs 18-20. Haplophragmoides d. concaVllS (Chapman). - Kuhnt, 1990, p. Kalamopsis grzybowskii (Dylqianka). - Charnock & Jones, 312, pI. 4, fig. 13. 1990, p. 151, pI. 1, figs 21-22; pl. 13, fig. 21. Kalamopsis grzybowskii (Dylqianka). - Kaminski & Geroch, Haplophragmoides horridus (Grzybowski, 1901) 1993, p. 281, pI. 17, figs 5a-8. Haplophragmoides llOrridlis (Grzybowski). - Kaminski et al., 1988, p. 189, pI. 5, fig. 11 a-b. Karreriella c11apapotensis (Cole, 1928) Haplophragmoides horridliS (Grzybowski). - Charnock & Jones, 1990, p. 170, pI. 5, figs 15-16; pI. 16, fig. 9. Karreriella chapapotensis (Cole). - Kaminski et al., 1990, p. 370, pl. 8, fig. 8. Haplophragmoides kirki Wickenden, 1932 Karreriella horrida Mjatliuk, 1970 Plate 2, Fig. 9 Plate 1, Fig. 8 Haplophragmoides kirki Wickenden. - King, 1989, p. 455, pI. 9.1, fig. 19. Karreriella horrida Mjatliuk. - Kaminski et al., 1988, p. 196, Haplophragmoides kirki Wickenden. - Charnock & Jones, pI. 9, figs 19-20. 1990, p. 170, pI. 5, figs 17-18; pI. 16, fig. 10. Karreriella horrida Mjatliuk. - Kaminski et al., 1990, p. 370, Haplophragmoides kirkl Wickenden. - Gradstein et al., 1994, pI. 8, figs 7-8. pl. 6, figs 1-6. Karrerulina IlOrrida (Mjatliuk). - Kaminski & Geroch 1993, p. 269, pI. 13, figs 14a-15b. Haplophragmoides d. kirki Wickenden, 1932 Karrerulina conifonnis (Grzybowski, 1898) Plate 2, Fig. 6 Karreriella coniformis (Grzybowski). - Kaminski et ai., 1988, Haplophragmoides d. kirki Wickenden. - Kaminski et ai., p. 195, pI. 9, f~gs 15-16. 1990, p. 368, pI. 5, fig. 3a-b. Karrerulina coniJormis (Grzybowski). - Charnock & Jones, 1990, p. 195, pI. 25, fig. 9. Coarser grained and somewhat larger than H. kirki KarreYllfina coniformis (Grzybowski). - Kaminski & Geroch, 1993, pp. 269-270, pl. 13, figs 1-4. Haplophragmoides porrectus Maslakova, 1955 Plate 2, Fig. 8 Karrerulina conversa (Grzybowski, 1901) Haplophragmoides porrectus Maslakova. - Kaminski et al., Plate 1, Figs 6, 7 1988, p. 189, pI. 5, figs 7-8. Karreriella conversa (Grzybowski). - Kaminski et al., 1988, Haplophragmoldes porrectus Maslakova. - Charnock & p. 196, pl. 9, figs 17-18b. Jones, 1990, p. 171, pl. 5, fig. 19. Kam:rulina cOl/versa (Grzybowski). - King, 1989, p. 456, pl. 9.2, figs 23, 24. Haplophragmoides stomatus (Grzybowski, 1898) Karreriella con versa (Grzybowski). - Kaminski, 1990, p. Plate 2, Fig. 7 370, pI. 8, fig. 5. Karrerlilina con versa (Grzybowski). - Charnock & Jones, Haplophragmoides stomatlls (qrzybowski). - Kaminski & 1990, pp. 195-196, pl. 12, fig. 19. Geroch, 1993, p. 264, pl. 11, fIgs 1a-2b. Karrerzdina conversa (Grzybowski). - Morlotti & Kuhnt, 1992, p. 222, pI. 4, fig. 15. Haplophragmoides suborbicularis (Grzybowski, 1896) Martinottiella communis (d'Orbigny, 1846) Plate 1, Fig. 9 Haplophragmoides suborbicularis (Grzybowski). - Charnock & Jones, 1990, p. 171, pl. 6, figs 1-2; pI. 17, fig. 1. Martinottiella commullis (d'Orbigny). - Schroder, 1986, p. 56, pI. 22, fig. II. Haplophragmoides walteri (Grzybowski, 1898) Martinoltiella communis (d'Orbigny). - King, 1989, p. 456, pl. 9.2, figs 4, 5. Plate 2, Fig. 5 Martinottie/la communis (d'Orbigny). - Bender, 1995, p. 46, Haplophragmoides walteri (Grzybowski). - Kaminski et al., pl. 6, fig. 16. 1988, p. 190, pI. 5, figs 14-15. Haylophragmoldes walteri. (Grzybowski). - Charnock & Paratrochammina challengeri Bronnimann & Jones, 1990, p. 171, pl. 6, fIgS 3-4. Whittaker, 1988 Haplophragmoldes walteri (Grzybowski). - Kuhnt, 1990, p. 314, pI. 4, figs 10-l2. Trochammina d. globigeriniJormis (Parker & Jones). - Haplophragmoldes walteri (Grzybowski). - Gradstein et al., Schroder, 1986, pp. 52-53. p1.I9, figs 5-8. 1994, pI 7 figs 1-5. Trochalllminopsis challengeri (Bronnimann & Whittaker). - Charnock & Jones, 1990, p. 189. pl. 11, figs 7-10. pl. 22. fig. Haplophragmoides walteri excavatus Cushman & 6. 234 Susan Kinsey
Paratroelwmmina challengeri Bronnimann & Whittaker. - pI. 1, figs 10-13. Jones, 1994, pp. 41-42, pI. 35, fig. 10. Rlwbdammilla excels a (Grzybowski). - Charnock & Jones, 1990, p. 152, pI. 1. figs 26-27, pI. 13. fig. 24. ReCllrvoides ex. gr. gerochi Pflaumann, 1964 Rhiza17lmilla illdivisa Brady. - Kuhnt, 1990, p. 324, pI. 1. fig. 13. Plate 4, Fig. 6 Rlziza17lmina illdivisa Brady. - Mariotti & Kuhnt, 1992, p. ReCllrvoides sp. var. geroelli Pflaumann. - Jones, 1988, p. 184, 223, pI. 2. fig. 4. pI. 2, fig. 4. Rzehakina minima (Cushman & Renz, 1946) Recllrvoides ex. gr. turbinatlls (Brady, 1881) Plate 1, Fig. 12 Plate 2, Fig. 12 RzeJzakina lIlinima (Cushman & Renz). - Kaminski et al., 1988, Recurvoides d. turbillatus (Brady). - Kaminski et al., 1988, p. p. 186, pI. 7, figs 8-9. 191, pI. 6, figs 8-9. RzeJzakina millima (Cushman & Renz). - Jones, 1988, p. 148, Recllrvoides ex. gr. tu!binatlls (Brady) .. - Charnock & Jones, pI. 2, fig. 2. 1990, p. 173, pl 6, fIgs 13-15, pI. 17, fIg. 8. RzeJzakilla millima (Cushman & Renz). - Charnock & Jones, 1990, p. 159, I?I. 3, figs 3-4; pI. 14, fig. 15. RzeJzakina mi1ll11la (Cushman & Renz). - Gradstein et al., Recllrvoides sp. 2 1994, pI. 9, figs 18-20. Plate 4, Fig. 2 Rzelzakilla epigona (Rzehak, 1895) Four elongated chambers in the last whorl. Sutures Plate 1, Fig. 14 generally flush. Small, the wall is smooth and RzeJzakill~ epigolla (Rzehak). - Kaminski et al., 1988, p. 186, finely grained. pI. 7, fIgs 6-7. Rzelzakina epigona (Rzehak). - Charnock & Jones, 1990, p. ReclIrvoides sp. 3 159, I?I. 3, figs 1-2; pI. 14, fig. 14. Plate 4, Fig. 3 Rzelzakma epigo11a (Rzehak). - Gradstein et al., 1994, pI. 9, figs 14-17. Quadrate outline with 7-8 'square' chambers in last whorl. Sutures slightly depressed. The wall is Saccam111ina placenta (Grzybowski, 1898) smooth and finely grained. Saccammizw placenta (Grzybowski). - Kaminski et al., 1988, p. 183, pI. 2, fig. 9. Sacca11lml11a placenta (Grzybowski). - Kuhnt, 1990, p. 325, ReticlIlophragmillm amplectens (Grzybowski, 1898) pI. 2, fig. l. Saccammma placenta. (Grz~bowski~. - Charnock & Jones, Plate 2, Figs 1, 2 1990, p. 147, pI. 1, fIgs 5-6; pI. 13, fig. 4. Reticliloplzragmimn amplectens (Grzybowski). - King, 1989, p. 458, pI. 9.2, figs 16-18. Sigmoilopsis schlll11lbergeri (Silvestri, 1904) Reticulopliragmium a11lplectens (Grzybowski). - Kaminski et aI., 1990,'p' 369, pI. 6, fig. 4a-b. Sigmoilopsis sclzilimbergeri (Silvestri). - Schroder, 1986, p. Cycla11l1lllna (Reticulopllragmillm) amplectells 56, pI. 21, fig. 9. (Grzybowski). - Charnock & Jones, 1990, p. 176, pI. 8, figs Sigmoilopsis sclziumbergeri (Silvestri). - King, 1989, p. 462, 1-5. pI. 9.3, figs 10, 11. Reticliioplzragmillll1 amplectells (Grzybowski). - Kaminski & Sigmoilopsis selliumbergeri (Silvestri). - Bender, 1995, p. 52, Geroch, 1993, p. 266, pI. 11, fIgs 5-7c. pI. 7, fig. 18, pI. 12, fig. 7. ReticlllopiJragmizl111 amplectens (Grzybowski). - Gradstein et ai., 1994, pI. 4, figs 1-5, pI. 5, figs 1-10. Spiroplectammina deperdita (D'Orbigny, 1846)
Spiroplectammilla (Spiroplectilleila) depe~dita (D'Orbi&ny). - Reticlllopltragmium intermedia (MjaUiuk, 1970) Charnock & Jones, 1990, p. 182, pI. 9, fIg. 14; pI. 21, fig. 4. Plate 2, Fig. 4 Spiroplectammina llavarroalla Cushman, 1932, Cyclammilla? intermedia Mjatliuk, 1970, p. 89, pI. 21, fig 6, pI. 28, fig. 1a-c. emend Gradstein & Kaminski, 1989 Plate 1, Fig. 5
Reticlliophragmoides jarvisi (Thalmann, 1932), Spiropiectammina na~arroalla Cushman. - Kaminski et al., emend Gradstein & Kaminski, 1989 1988, p. 193, pI. 7, fIgs 13-15. Spiropiectmmnilla navarroana Cushman, emend Gradstein & Reticuioplzragmoides jarvisi (Thalmann), emend Gradstein & Kaminski, - Gradstein & Kaminski, 1989, pp. 83,85. pI. 9. Kaminski, 1989, PI? 81, 83, pI. 7, figs 1-8, text-fig. 4. figs 1-12, text-fig. 5. Reticuioplzragmoides Jarvisi (Tfialmann), emend Gradstein & Spiroplectammina (Spiroplectammina) navarroana Cushman, Kaminski. - Charnock & Jones, 1990, p. 177, pI. 8, figs 12- emend Gradstein & Kaminski. - Charnock & Jones, 1990, 13, pI. 19, fig. 4. I? 181, pI. 9, figs 11-12; pI. 21, fig. 1. RetiCll1oplzragmoides jarvisi (Thalmann), emend Gradstein & Splropiectammilla navarroana Cushman, emend Gradstein & Kaminski. - Gradstein et al., 1994, pI. 7, figs 10-11, pI. 11, Kaminski. - Gradstein et ai., 1994, pI. 1, fig. 12a,b, pi 11, fig. 6. figs 11-12.
Rhabdammina abysorrllm Sars, In Carpenter, 1869 Spiroplectammina spectabilis (Grzybowski, 1898) Plate 1, Fig. 11 Plate 1, Figs 1-3 Rhabdammina abysorrzmz Sars, In Carpenter. - Charnock & Spiroplectammilla spectabilis (Grzybowski). - Kaminski et Jones, 1990, p. 152, pI. 1, figs 23-24, pI. 2, fig. 9, pI. 13, fig. ai., 1988, p. 193, pI. 7, figs 16-18. 22. Spiropiectammina (Spiroplectinelia) spectabilis (Grzybowski). - Charnock & Jones, 1990, pp. 182-183, pI. 9, figs 15-18. Rhabdammina excelsa (Grzybowski, 1898) Spiroplectam1llilla spectabilis (Grzybowski). - Kaminski & Rhizammina illdivisa Brady. - Kaminski et ai., 1988, p. 183, Geroch, 1993, pp. 267-268, pI. 12, figs 4a-5c. Palaeogene benthic foraminifera of the Halten Terrace, Norway 235
Trochamminoides irregularis (White). - Kaminski et al., Spirosigmoilillella compressa Matsunaga, 1955 1988, p. 191, pI. 4, fig. 18. Plate 1, Figs 13, 15 Trochamminoides irreglilaris (White). - Kuhnt, 1990, p. 320, pI. 5, fig. 10. Spirosigmoilillella COlllpressa Matsunaga. - Charnock & Jones, 1990, p. 159, pI. 3, figs 5-6; pI. 14, fig. 16. Spirosigmoilinella compressa Matsunaga. - Kaminski et al., Trocllammilloides proteus (Karrer, 1866) 1990, p. 367, pI. 4, figs 1-2. Trochammilloides proteus (Karrer). - Kaminski et al., 1988, p. 192, pI. 4, fig. 20. Sllbreophax scalaris (Grzybowski, 1896) Trochaml1linoides proteus (Karrer). - Kuhnt, 1990, p. 326, pI. 5, fig. 10. _ Subreoplzax scalaris (Grzybowski). - Kaminski et al., 1988, p. Troclzal1lminoides proteus (Karrer). - Charnock & Jones, 187, pI. 2, figs 16-17. 1990, p. 161, pI. 3, fig. 12; pI. 15, fig. 2. Sllbreophax scalaris (Grzybowski). - Kuhnt, 1990, p. 326, pI. 3, figs 4-5. Troc1zammilloides sllbcorollatlls (Grzybowski, 1896) Subreoplzax scalaris (Grzybowski). - Morlotti & Kuhnt, 1992, p. 223, pI. 3, fig. 5. Trocllllmminoides sllbcoronatus (Grzybowski). - Kaminski et al., 1988, p. 192, pI. 4, fig. 20. Trochammilla altiforntis (Cushman & Renz, 1946) Trochamminoides subcoronatlls (Grzybowski). - Morlotti & PIa te 2, Fig. 11 Kuhnt, 1992, p. 223, pI. 3, fig. 13. Troc/zammina aItiformis (Cushman & Renz). - Kaminski et al., Trochammillopsis pselldovesicularis 1988, p. 193, pI. 8, figs 1a-2b. (Krasheninnikov, 1974) Trochammilla deformis Grzybowski, 1898 Troclzamminopsis pseudovesiwlaris (Krasheninnikov). - Charnock & Jones, 1990, p. 189, pI. 22, fig. 7. Troc/zaml1lina deformis Grzybowski. - Kaminski et al., 1990, p. 369, pI. 7, fig. 1a-c. ACKNOWLEDGEMENTS Trochammilla ntthVellmllrrayi Cushman & Renz, I gratefully acknowledge the financial support of 1946 the BMFT and STA TOIL. ST A TOIL also provided Plate 4, Figs 10, 12 all the sample material. Troc/lammina Tllthven-Jllurrayi Cushman & Renz. - Kaminski I am grateful to Prof. Dr. J. Thiede for giving me et al., 1988, p. 193, pI. 8, fig. 6a-c. the opportunity to carry out my Ph.D. research at Trochaml1lina Tlltlzvenmurrayi Cushman & Renz. - King, GEOMAR, in Kiel and for his support and guidance 1989, p. 460, pI. 9.3, figs 3,4. Trochammina (Ammoallita) TIIthvenmurrayi Cushman & during this study. Thanks also to my colleagues on Renz. - Charnock & Jones, 1990, p. 186, pI. 10, figs 4-9; pI. this project Dr. M. Weinelt and Dr. A. Aichinger 22, fig. 2. Many people helped me in identifying my micro fossils especially Dr. F.M. Gradstein, Dr. M.A. Trochammilla sllbvesicularis HanzHkova, in Kaminski, Prof. Dr. W. Kuhnt, Prof. J. Nagy, and Dr. Homola & Hanzlfkova, 1955 D. Spiegler. Plate 4, Fig. 11 Mr. A. v. Doetinchem helped with the electron Trochammilla (Insculptarellllla) subvesicularis Hanzlfkova, microscope and Ms. J. Heinze produced the photo in Homola & Hanzlfkova. - Charnock & Jones, 1990, p. 187, pI. 10, figs 10-12; pI. 22, fig. 3. graphs. Special thanks go to Bettina Ki.ibler for all Trochammina d. subveslcularis Hanzlfkova, in Homola & her technical help. Last but not least many thanks to Hanzlfkova. - Gradstein et al., 1994, pI. 1. fig 4-5. Drs Mike Charnock and Felix Gradstein for their The assemblages studied may also contain specimens very helpful and thoughtful reviews. of Ammollita illgerlisae Gradstein & Kaminski (1997), (F. Gradstein, pers. comm., 1997). REFERENCES Bender, H. 1995. Test structure and classification in aggluti Trochammina sp. 5 nated foraminifera. In: M.A. Kaminski, S. Geroch, & M.A. Plate 4, Figs 4-5 Gasinski (eds)., Proceedings of the Fourth International Workshop 011 Agglutinated Foraminifera. Grzybowski Small, plano-convex with 7 chambers in final Foundation Special Publication 3, 27-70. B0en, F., Eggen, S., & Vollset, J. 1984. Structures and basins whorl. Sutures are curved and slightly depressed. of the margin from 62N to 69N and their development. In: Wall is finely grained. Probably Trochammina sp. 2 A. M. Spencer (ed.), Petroleum Geology of the North Charnock & Jones 1990, p. 188, pI. 11, figs 11-12. pI. European Margin., Norwegian Petroleum Society, 253- 23. fig. 1. (M. Charnock, pers. comm., 1998) 270. Bohrmann, G., Henrich, R., and Thiede, J. 1990. Miocene to Quaternary Paleoceanography in the Northern North Trochammilloides dllbillS (Grzybowski, 1898) Atlantic: Variability in Carbonate and Biogenic Opal Plate 4, Fig. 7 Accumulation. In: U. Bleil and J. Thiede. (eds). GeologIcal History of the Polar Oceans: Arctic versus Antarctic. Trochlllnminoides dl/bius (Grzybowski). - Kaminski et al., NATO ASI Series. Series C, Mathematics and Physical 1988, p. 191, pI. 4, figs 16-17. Sciences. Kluwer Academic Publishers, 647-675. Trochamminoiaes dl/bllls (Grzybowski). - Kuhnt, 1990, p. Charnock, M.A. & Jones, R.W. 1990 Agglutinated 326, pI. 5, fig. 9. foraminifera from the Paleogene of the North Sea. In: C. Trochamminoldes dubius (Grzybowski). - Kaminski et al., Hemleben, M.A. Kaminski, W. Kuhnt, & D.B Scott. (eds) 1996, pI. 3, figs 1-4. Paleoecology, Biostratigraphy, Paleoceanography and Trochammilloides irreglliaris (White, 1928) Taxonomy of Agglutinated Foraminifera. NATO Plate 4, Fig. 8 Advanced Studies Institute, Series C, Mathematics and Physical Sciences, Kluwer Academic Publishers, 327, 236 Susan Kinsey
433-506. 345-386. Dalland, A, Worsley, D., Ofsted, K. 1988. A Lithostrati Kaminski, M.A., & Geroch, S. 1993 A reVISIOn of graphic scheme for the Mesozoic and Cenozoic foraminiferal species in the Grzybowski Collection. In: succession offshore mid- and northern Norway. M.A. Kaminski, S. Geroch & D.G. Kaminski, (eds), The Norwegian Petroleum Directorate Bulletin, 4, 65 pp. Origins of Applied Micropaleontology: The School of Eldholm, 0., Thiede, E., & Taylor, E. 1989. The Norwegian Josef Grzybowski. Grzybowski FoundatioJl Special continental margin: tectonic, volcanic and paleonviron Publication, 1, Alden Press, 239-324. mental framework. In: O. Eldholm, J. Thiede, E. Taylor, et King, e. 1983. Cainozoic micropaleontological biostratigra al.. (e~s), Proceedings of the Ocean Drilling Program, phy of the North Sea. Reports Institute Geological Science, SCientifIc Results 104, College Station, TX, 5-26. 82 (7), 1-40. Gradstein, F.M., Kaminski, M.A., Berggren, W.A., King, e. 1989. Cenozoic of the North Sea. In: D.G. Jenkins & Kristiansen, I.L & D'Ioro, M.A. 1994. Cenozoic J.W. Murray, (eds), Stratigraphical Atlas of Fossil biostratigraphy of the North Sea and Labrador Shelf. Foraminifera. Ellis Horwood Ltd. Chicester, 418-489. Micropalaeontology, 40 supplement, 152 pp. Kristoffersen, Y. 1990. On the tectonic evolution and paleo Gradstein, F., & Backstrom, S. 1996. Cainozoic biostratigra ceanographic significance of the Fram Strait gateway. In: phy and palaeobathymetry, northern North Sea and U. Bleil & J. Thiede, (eds). Geological History of the Polar Haltenbanken. Norsk Geologisk Tiddskrift, 76, 3-32. Oceans: Arctic versus Antarctic. NATO ASI Series. Series Gradstein, F., & Kaminski, M.A. 1989. Taxonomy and C, Mathematics and Physical Sciences. Klewer Academic biostratigraphy of new and emended species of Cenozoic Publishers, 63-76. deep-water agglutinated foraminifera from the Labrador Kuhnt, W. 1990. Agglutinated foraminifera of western ana North Seas. Micropaleontology, 35, 72-92. Mediterranean Upper Cretaceous pelagic limestones Gradstein, F., & Kaminski, M.A. 1997. New species of Umbrian Appenines, Italy, and Betic Cordillera, Southern Paleogene deep-water agglutinated foraminifera from the Spain. Micropaleontology, 36 (4), 297-330. North Sea and NorwegiJn Sea. Annales Societatis Labude, e. 1984. Sedimentologie, Substanz und die verbreit Geologorll1n Poloniae. 67, 217-229. ung sandschaliger und planktonischer Foraminiferen im Hamer, G., & Hjelle, K. 198-l. Tectonic framework of the Maastricht des Zentralen Apennin Italien. Tiibinger More Basin and the northern North Sea. In A.M. Spencer Mikropalaontologische Mitteil1lng, 2, 95 pp. (ed.), Petroleum Geology of the North European Margin, Loeblich, A.R. & Tappan, H. 1987. Foraminiferal Genera and 349-358. their Classification. 2 vols., 1182 pp., Van Nostrand Holtedahl, H. 1993. Marine Geology of the Norwegian Reinhold, New York. Continental Margin. Norges Geologiske Undersalkelse, Miller, K.G., & Tucholke, B.E. 1983. Development of Special Publication, 6, 150 pp. Cenozoic abyssal circulation south of the Greenland Hull, D.M. 1996. Paleoceanography and biostratigraphy of Scotland ridge. In: M. H. P. Bott, M. Talwani, J. Thiede, & Paleogene radiolarians from the Norwegian-Greenland S. Saxov, (eds), Structure and development of the Sea. In: J. Thiede, A.M. Myhre, J.V. Firth et al., (eds) Greenland-Scotland ridge. New methods and concepts. Proceedings of the Ocean Drillillg Program, Sciel1tific New York: Plenum Press, 549-590. Results, 151, College Station, TX, 125-146. Mjatliuk, E.V. 1970. Foraminifery flischevykh otlozhenii Jones, G.D. 1988. A paleoecological model of late Paleocene vostochnykh Karpet (Mel-Paleogen). T r u d y Flysch-type agglutinatea foraminifera using the Vsesoyuznogo Neftyanago. Naucll11o-Issledovatel'skogo Paleoslope transect approach, Viking Graben, North Sea. Geologo-Razvedochnogo Instltuta, 282, 358 pp. In: F. Rogl & F. M. Gradstein, (eds), Proceedings of 2nd Morlotti, E., & Kuhnt, W. 1992 Agglutinated deep water workshop on Agglutinated Foraminifera. Ablwndllmgen foraminifera of the Eocene Monte Piano Formation Geologisc7Je Bundesa1lstalt, 41, 143-153. Northern Arpenines, Italy. Journal of Foraminiferal Jones, R.W. 1994. The Challenger Foramillifera, 149 pp. Research, 22 (3), 214-228. Oxford University Press, Oxford. Myhre, A.M., Eldholm, 0., Faleide, J.I., Skosgeid, J., Kaiho, K. 1991. Global changes of Paleogene aero Gudlaugsson, S.T., Planke, S., Stuevold, L.M., & Naagnes, bic/anaerobic benthic foraminifera and deep-sea circula E. 1992. Norway- Svalbard continental margin: tion. Palaeogeography, Palaeoclimatology, Palaeoecology, structural and stratigraphical styles. In: e.W. Poag & P.e. 83 (1-3),65-86. Gracinsky, (eds)., Geologic Evol1ltion of the Atlantic Kaminski, M.A., Gradstein, F.M., & Berggren, W.A. 1989a. Continental Rises. New York Van Nostrand Reinhold, Paleogene benthic foraminiferal biostratigraphy and 157-185. paleoecology at site 647, Southern Labrador Sea. Ill: S.P. Nagy, J., Kaminski, M.A. Johnsen, K., & Mitlehner, A.G. Srivastava, M.A. Arthur, B. Clement, et a!. (eds), 1997. Foraminiferal, palynomorph, and diatom Proceedings of the Ocean Drilling Program, Scientific biostratigraphy and Paleoenvironments of the Torsk Results, 105, College Station TX, 705-730. Formation: A reference section for the Paleocene-Eocene Kaminski, M. A., Gradstein, F. M., Berggren, W.A., Geroch, transition in the western Barents Sea. In: e. Hass, & M.A. Kaminski, (eds). S., & Beckman, J. P. 1988. Flysch -type agglutinated assem Micropaleontology alld Paleoceanography blages from Trinidad: Taxonomy, Stratigraphy, and of the northern North Atlantic. Grzybowski Foundation Paleobathymetry. In: F. Rogl & P.M. Gradstein (eds), Special Publication,S, 15-38. Proceedings of 2nd workshop on Agglutinated Osterman, L.E., & Spiegler, D. 1996. Agglutinated benthic Foraminifera. Abhandlungen Geologische B1Indesanstait, foraminiferal biostratigraphy of Sites 909 and 913, 41, 155-228. Northern North Atlantic. In: J. Thiede, A.M. Myhre, J.V. Kaminski, M.A., Gradstein, F.M., Scott, D.B., & Mackinnon, Firth et a!., (eds) Proceedings of the Ocean Drilling K.D. 1989b. Neogene benthic foraminifer biostratigraphy Program, Scientific Results, 151, College Station, TX, 169- and deep water nistory of sites 645, 646 and 647, Baffin 185. bay and Labrador sea. In: S.P. Srivastava, M. Arthur, B. Pardo, A., Keller, G., Molina, E., Canudo, J.1. 1997. Planktic Clement, et. al. (eds), Proceedings of the Ocean Drilling foraminiferal turnover across the Paleocene-Eocene Program, Scientific Results, 105, College Station, TX, 731- transition at DSDP Site 401, Bay of Biscay, North 756. Atlantic. Marine Micropaleontology, 29, 129-158. Kaminski, M.A., Gradstein, F.M., Goll, R.M., & Greig, D. Schroder, e. 1986. Deep-water Arenaceous Foraminifera in 1990. ~iostratigraPJ:Y. and Paleoeco.logy of deep-water the Northwest Atlantic Ocean. Canadian Tee/mical Report agglutmated foraminifera at ODP site 643, Norwegian of Hydrology and Ocean Sciences, 71, 191 pp. Greenland Sea. In: e. Hemleben, M.A. Kaminski, W. Steurbaut, E., Spiegler, D., Weinelt, M. & Thiede, J. 1991. Kuhnt, & D.B. Scott, (eds), Paleoecology, Biostratigraphy, Progress report for April 1991 to December 1991 of Paleoc~anography and Taxonomy of Agglutillated project "Cenozoic erosion and sedimentation on the Forammifera. NATO ASI Series C, Mathematics and Northwest Euro);ean continental margin and Adjacent Physical Sciences, Kluwer Academic Publishers, 327, areas" within 'German-Norwegian co-operation in Palaeogene benthic foraminifera of the Halten Terrace, Norway 237
geosciences". - IntcrIll1/ Report Kiel, GEOMAR, 30 pp. Thiede, J., & Myhre, A.M 1996b. The Paleoceanographic his Stuevold, L.M. & Eldholm, O. 1996. Cenozoic uplift of tory of the North Atlantic-Arctic gateways: Synthesis of Fennoscandia inferred from a study of the mid the Leg 151 drilling results. In: J. Thiede, A.M. Myhre, J.V. Norwegian margin. Globl11l1nd Planetary Change, 12, 359- Firth et aI, (eds), Proceedings of the Ocean Drilling 386. Program, Scientific Results, 151, College Station, TX:, Talwani, M., & Eldholm, O. 1977. Evolution of the 645-658. Norwegian-Greenland Sea. Geological Society of America Tucholke, B.E. & Mountain, G.S. 1986. Tertiary paleoe Bulletin, 88, 969-999. ceanography of the western North Atlantic Ocean. In: Thiede, J., & Myhre, A.M. 1996a. Introduction to the North P.R. Vogt & B.E. Tucholke. (eds), The Geology of North Atlantic-Arctic Gateways: Plate Tectonic-Paleoceano America, The Western Atlantic region. Vol. M, Geological graphic History and Significance. In: J. Thiede, A.M. Society of America Memoir, 631-650. Myhre, J.V. Firth et ai., (eds), Proceedings of the OCel111 Drilling Program, Scientific Results, 151, College Station, TX,3-23.
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EXPLANA nONS TO PLATES
PLATE 1. 1. Spiroplectammina spectabilis, Well 6406/11-1, IS90m, x3S. 2. Spiroplectammina spectabilis, Well 6407/7-2, 1970m, xS6. 3. Spiroplectammina spectabilis, Well 6406/11-1, 2330m, x42. 4. Bigenerina sp. I, Well 6407/7-2, 19S0m, xS6. 5. Spiroplectal1lmina navarroana,Well 6406/11-1,21S0m, x46. 6. Karrerulina conversa, Well 6407/7-2, 1760m, x42. 7. Karrerulina conversa, Well 6406/11-1,23S0m, x3S. 8. Karreriella horrida, Well 6407/7-2, 1760m, xS6. 9. Martinottiella communis,Well 6406/S-1, 16S0m, x23. 10. Bathysiplwn sp., Well 6406/S-1, 2760m, x29. 11. Rhabdammina abyssorum, Well 6406/11-1, 23S0m, x60. 12. Rzehakina minima. Well 6406/11-1, 2260m, x69. 13. Spirosigmoilinella compressa, Well 6407/7-2, 1240m, xSS. 14. Rzehakina epigona, Well 6406/S-1, 2710m, x7S. 15.Spirosignzoilinella compressa, Well 6406/S-1, 19S0m, x71. 16. ?Tllrrilina alsatica, Well 6406/11-1, 14S0m, x17S.
PLATE 2. 1. Reticlilophragmillm amplectens, Well 6407/7-2, 1760m, x4S. 2. Reticlliophragmium amplectens, Well 6407/7-2, IS70m, x60. 3. Cyclanzmina placenta, Well 6406/11-1, 1760m, xIS. 4. Reticlilophragmillm intermedia, Well 6407/7-2, IS70m, xS6. 5. Haplophragmoides walteri, Well 6406/S-1, 2710m, x112. 6. Haplophragmoides cf. kirki, Well 6407/9-3, 1300m, x110. 7. Haplophragmoides stomatus, Well 6407/7-2, 1760m, xS3. 8. Haplophragmoides porrectus, Well 6407/7-2, 1710m, x122. 9. Haplophragmoides kirki, Well 6406/11-1, 22S0m, x116. 10. Haplophragmoides sp. 2, Well 6407/7-2, 1670m, x79. 11. Trocizammina altiformis,Well 6407/7-2, 1730m, xSS. 12. ReCllrvoides ex gr. tllrbinatus, Well 6407/7-2, I9IOm, x64.
PLATE 3. 1. Ammodiscus cretaceus, Well 6407/7-2, 19S0m, x49. 2. Ammodiscus tenuissimus, Well 6407/7-2 1710m, xISO. 3. AmmodisClls pennyi, Well 6407/7-2, 1720m, x60. 4. Glomospira cizaroides,Well 6407/9-3, 960m, x9S. 5. Cystammina pauciloculata/C. sveni, Well 6407/7-2, 1720m, x90. 6. Glomospira glomerata,Well 6406/S-1, 20S0m, x27. 7. Cystal1lmina pauciloclliata/C. sveni. Well 6407/7-2, 1760m, xS6. 8. Cystalllmina pallciloculata/C. sveni Well 6407/7-2, 1760m, x7S. 9. Glol1lospira c/zaroides, Well 6407/9-3, 960m, x120. 10. Cribrostomoides sp. I, Well 6407/7-2, 1670m, x144. 11. Cribrostomoides sp. I, Well 6407/7-2, I670m, x121. 12. Al1lmomarginulina aubertae, Well 6407/7-2, I670m, x9S.
PLATE 4. 1. Adercotrynza agterbergi,Well 6407/7-2, 16S0m, x64. 2. Recurvoides sp. 2, Well 6407/7-2, 12S0m, x13l. 3. Recurvoides sp. 3, Well 6407/7-2, I930m, x4S. 4. Trochal1ll1lina sp. S, Well 6406/S-1, 24S0m, x13l. 5. Trochammina sp. S, Well 6406/S-1, 24S0m, x116. 6. Recurvoides ex. gr. gerochi,Well 6407/7-2, 19S0m, xS3. 7. Trocizamminoides dllbius, Well 6407/9-3, 12S0m, x71. 8. Trochamminoides irregularis, Well 6407/9-3, I410m, xSO. 9. Conglophragmillm corona tum, Well 6407/7-2, 1740m, x27. 10. Trochammina ruthvenmurrayi, Well 6407/9-3, 1440m, x46. 11. Trochammina subvesicularis,Well 6407/7-2, 1910m, x92. 12. Trochammina ruthvenmurrayi, Well 6406/11-1, 2310m, x7S. S.... nKI~
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