The type section of the Vikinghggda Formation: a new Lower Triassic unit in central and eastern Svalbard
ATLE MGRK, GEIR ELVEBAKK, ARNE W. FORSBERG, MARK W. HOUNSLOW. HANS ARNE NAKREM. JORUNN 0s VIGRAN and WOLFGANG WEITSCHAT
L Mcnrk, A,, Ehehakk, G., Forsberg, A. W., Hounslow, M. W., Nakrem, H. A,. Vigran, J. 0. & Weitschat. W. 1999: The type section of the Vikinghogda Formation: a new Lower Triassic unit in central and eastern Svalbard. Polirr Resi~orchI&lJ, 51-XI. The Vikinghogda Formation (250 in) is defined with a stratotype in Deltadalen-Vikinghcngda in central Spitsbergen. The Vikinghogda Formation replaces the Vardebukta and Sticky Keep Formations of Buchan -U+P~~~~~NS''et al. (1965) and the lower part of the Barentscnya Formation of Lock et al. (1978) a!, extended geographically by Mvcrk, Knarud et al. (1982) in central Spitsbergen, Barentscnya and Edgecnya. The formation consists of three member\: the Deltadalen Member (cornposed of mudstones with sandstones and siltstones), the Lusitaniadalen Meinher (dominated by mudstones with thin siltstone beds and some limestone concretions) and the Vendorndalen Member (composed of dark shales with dolomite interbeds and nodules). The Lu,itaniadalen and Vendomdalen members replace the former Sticky Keep Formation/ Member in the siirne areu. The Vikinghogda Formation can be followed through central and eastern Spitsbergen to Barentseya and Edgecrya and includes all sediments between the chert-rich Kapp Starostin Formation (Permian) and the organic-rich shales of the Botneheia Formation (Middle Tri subdivision into three members is :itso reflected in the organic carbon content and palynofacies. Upwards. each succeeding member becomes inure distal, organic-rich and oil-prone than the one helow. The Vikinghegda Formation is well-dated by six ammonoid zones. although the transitional beds between the Deltadalen and Lusironiadalen members lack age diagnostic macrofossils. Corresponding palynozonation and magnetustratigraphy have also been determined. The overall stratigraphical development correlates well with other key Triassic mas in the Arctic, although intervals in the late Dienerian and early Smithian may bt. condensed or missing.
Ar/e Mgrk, IKti/SINTEF Pi,rri)/ivtni R<,.WU~C/?.N- 7465 Trundheini. Nor?wy: Geir Elcehnkk. Saga Pefro/eirm ASA, P.O. B(1.r 113-1, N-9401 H~irsrizd,Norwny; Anw W. Forsberg, Norsk Hydro ASA. P.O. BOA -700 N- 132/ Smhekk, Nunvuy: Mark W.Horindi~w. .khiio/ of Eiwironnwnrnl Sciences, UniwrAiry cf Eosf Atigliu, Nonvich, NR4 7TJ. UK; Hi7n.c Arne Ntrkrcni. Pu/eiiritologicu/ Mirsrunt. tiniwrsity if Odo, Sursgr. I, N- 0502 Os/iJ5, Ni)nr.n,v; Jorrrnn OS l'iqrcni. Hans H~gerripsgt.10. N-7012 Trondheirn, Norway: WolfKntig Wrifschur.G'ri~lo~ic~ul-P~r/nci~nti~/i~,~i~~o/ Instirrife inid Musewn. Uniivrtity o$ Hanhirg, Bundessrr. 55. D- 20146 Hunfhr~.Genncrn,v.
Introduction unit on the map series of the Norwegian Polar Institute (Major et al. 1992; Miloslavskij, Birju- The Lower and Middle Triassic succession of kov. Slenskij. Hansen et al. 1993; Miloslavskij. Svalbard consists of fine-grained clastics. The Birjukov, Slenskij & Dallmann 1998). The dominant sediment supply from the west resulted lithological and sedimentological description of in extensive deposits of coastal and shallow the Vikinghogda Formation type section is sup- marine sandstones and shales in western Spitsber- plemented with biostratigraphical dating (macro- gen, whereas shales with minor siltstones and fossils and palynology), magnetostratigraphy, and sandstones were deposited in a basinal setting in organic geochemical screening analyses. central and eastern Spitsbergen, Barentsoya and Edgeoya (Fig. 1). This sedimentary pattern con- Lithostratigrciphical review: The Lower and tinues southwards under the Barents Sea, with Middle Triassic succession of Svalbard, the deposition of shales in basins and coarser grained Sassendalen Group, was originally subdivided clastics along the basin margins and on local highb. into the Vardebukta (Induan), Sticky Keep The Viliinghmgda Formation. formally defined (Olenekian) and Botneheia (Anisian and Ladi- here. comprises Lower Triassic sediments in nian) formations by Buchan et al. (1965; Fig. 2). It central and eastern Spitsbergen, Barentsoya and was based on coastal and mountain exposures Edgeoya and has served as a practical mapping around Isfjorden. This nomenclature was followed 52 A. M@rk et al.
nomenclature for the whole Triassic succession of Barents@yaand Edgeoya. These authors postu- lated that no subdivision was practical in these islands, and grouped all the sediments of the Sassendalen Group into the Barentsoya Formation, although they recognized the upper dark shales (the “oil shales member” of Falcon 1928), as forming a separate member. The shale-dominated Sassendalen Group sediments on eastern Spitsber- gen, Barentsoya and Edgeoya show close simila- rities, that can be followed to central Spitsbergen and to the south-western part of Nordaustlandet, as shown by M@rk& Worsley (figure 7 in M~rk& Worsley 1979) and PEelina (1983). Against this background, M@rk,Knarud et al. (1982) extended the Barentsoya Formation, as defined by Lock et 779 al. (1978), to central and eastern Spitsbergen. In addition, they retained the units as defined by Buchan et al. (1965) as members, and they had to rename the lower unit the Deltadalen member as the Vardebukta Formation was retained for its type Fig. I. Triassic exposures in Svalbard (black). Square indicates area in western Spitsbergen. the detailed map of Fig. 3. However, PEelina (1983) retained the Varde- bukta Formation for the central and eastern areas, but assigned the equivalent of the Sticky Keep on the map sheets, although the Sticky Keep and FormatiodMember to the Wichebukta Formation Botneheia formations were grouped together as with a type section at Teistberget on eastern the Kongressfjellet Subgroup (Flood et al. 1971a; Spitsbergen. PEelina also retained the Botneheia Major & Nagy 1972). Buchan et al. (1965) Formation with formational status in the same defined the Vardebukta Formation with a type areas, although she followed Mork, Knarud et al. section at Festningen in western Spitsbergen and (1982) and kept the Bravaisberget Formation for the Sticky Keep Formation with a type section at the equivalent beds in western Spitsbergen (Fig. 2). Vikinghogda in central Spitsbergen. The Committee on the Stratigraphy of Svalbard In the Hornsund area the local lithostratigraphy (Mork. Dallmann et al. in press) suggests that the defined by Birkenmajer (1977) was later modified organic-rich phosphate-bearing shales defined as and incorporated into the general scheme erected the Botneheia Formation by Buchan et al. (1965) for central Spitsbergen during the reappraisal of should retain formational status, as suggested by southern Spitsbergen by Worsley & Mork (1978). PEelina (1983). It will consequently replace the Mork & Worsley (1979) subsequently applied the upper part of the Barentsoya Formation of Lock et stratigraphical scheme of Buchan et al. (1965) to al. (1978) and Mork, Knarud et al. (1982), and the entire Svalbard archipelago. prompt the need for a new formational unit for the In the eastern islands, Barentsoya and Edgeoya, underlying part of the Sassendalen Group. extensive fieldwork by CASP (Cambridge Arctic The boundary between the two lower units of Shelf Programme) and Norwegian Polar Institute the Sassendalen Group has traditionally been geologists resulted in the preliminary map and regarded as corresponding to the InduadOlene- stratigraphy of Flood et al. (1971b), adapting the kian boundary. According to traditional western principles used for Spitsbergen, although with boreal terminology, this boundary corresponds to lowered rank (i.e. Kongressfjellet Formation and the DieneriadSmithian transition (Lower and Sticky Keep and Botneheia members). This Upper Scythian: Buchan et al. 1965; Induan to nomenclature was followed on the published Olenekian: PEelina 1965, 1967, 1977, 1983; 1 :500 000 map (Winsnes 1981). A more compre- KorEinskaja 1982; Dienerian to Smithian: Tozer hensive description was given by the CASP group, & Parker 1968; M@rk,Knarud et al. 1982; Mork, with Lock et al. (1978) introducing a local Embry et al. 1989; Mark, Vigran et al. 1993; Early Triassic lithostratigraphical units of Svalbard and the Barents Shelf I
~ Central-East Central-East Central-East Svalbard Hornsund Barentseya Western Spitsbergen Spitsbergen Spitsbergen lamrnerfest Svalis Western Spitsbergen a Area Edgeeya Spitsbergen BEyg$a West - South BarentsBYa Basin Dome Spitsbergen @?,",$'a -J Edge0ya Me* and Buchan et al. Birk;wTjer Locket al. Melk st al. 1971a 1971b I PEeline vorsley et a!. Elvebakk This work 1978 1982 1983 1988 8 I I 1999
Van Keulen- a 1-fjorden Fm. I 3 0 c L ,,, ,,, Botne- Botne- Botneheia n heia m heia Fm. c s Fm. E Mb. 1 1 L v) 0 U.
t Vendorn- C Ka .-m Mb Sticky Keep - Q) Fm. IS. 0 dalen B Mb t t Varde- Varde- Varde- Delta- Vardebukta 3 bukta dalen - Fin.
Is. = lskletten Member Ka. = Kaosfjellet Member
Fig. 2. Lithostratigraphical units used in the Lower and Middle Triassic succession. 54 A. MGrk et al.
Hochuli et al. 1989; and on numerous maps). The shore exposure as belonging to their Vardebukta general description of these lower and upper units Formation, and Xenoceltites sp. was reported from by all authors, has followed the same general this exposure. We have also found numerous principles, however the application of these examples of Arctocerus sp. in limestone nodules in definitions has not been straightforward, and this sea cliff, which shows that the exposure should misinterpretations have been inherited from paper be included in the Lusitaniadalen Member as to paper. Mark, Embry et al. (1989), Mark, Egorov defined herein. However, at Tschermakfjellet, the et al. (1994) and Mark (1994) interpreted a major situation is the reverse. Here the base of a cliff circum-Arctic transgression as early Olenekian in 60 m above the top of the Permian was regarded as age, and Vigran et al. (1998) and Van Veen et al. the base of the former Sticky Keep Formation, an ( 1993) reported a pronounced transgression early interpretation also followed by Mark, Knarud et al. in the Spathian in the western Barents Sea, similar ( 1982). This cliff consists of fine-grained, hum- to that reported by Embry (1988, 1997) in the mocky laminated sandstone quite similar to that of Sverdrup Basin. These transgressions around the the new type section, and the base of the Dienerian-Smithian boundary have all been cor- Lusitaniadalen Member should accordingly be related with the change from the Deltadalen moved to the top of this cliff. Member to the overlying unit. Buchan et al. (1965) subdivided their Sticky In the type section at Vikingh~gda and the Keep Formation into the Iskletten and Kaosfjellet neighbouring mountain Sticky Keep, Buchan et al. members with type sections on western Spitsber- (1965) defined the base of the Sticky Keep gen, and these are retained as subdivisions of the Formation at the first exposure above the scree- equivalent Tvillingodden Formation in the outer covered interval (i.e. at 115 and 129 m respec- Isfjorden area (Mark, Dallmann et al. in press). tively). In the type section in Deltadalen, Mark, The Lusitaniadalen and Vendomdalen members, Knarud et al. (1982) defined the boundary between as defined below, are regarded as directly the Deltadalen and Sticky Keep members 126m correlative to these members. above the base of the Triassic. This boundary is The establishment of the new Vikinghagda situated in the middle part of the well-defined Formation is warranted for several reasons: Euflemingites romunderi Zone. No palaeontologi- cal study was carried out in the 1982 work and the 1) The Vikinghagda Formation is the natural boundary was partly based on the old interpreta- mapping unit for the Lower Triassic sediment of tion of the nearby Sticky Keep section of Buchan central and eastern Svalbard. et al. (1965). This misinterpretation was trans- 2) Re-establishing the Botneheia unit as a forma- ferred to Stensiofjellet where a correlative bound- tion demands a new name for the underlying part ary was also drawn too high (figure 5 in Mark, of the previous Barentsaya Formation. Knarud et al. 1982). 3) The new name Vikinghagda is introduced The new palaeontological evidence, and the because the Vardebukta Formation is now re- improved understanding of the boundary criteria stricted to the western areas. Other names used also indicate that the boundary at Hagrinden on either comprise a larger rock volume (Barentsaya Barentsaya and Veidebreen on Edgeaya are drawn Formation), or a smaller or different volume too high. This interpretation is supported by the (Sticky Keep, Kongressfjellet and Wichebukta fauna reported from Kroki on central Edgeaya by units). PEelina (1 977) and by our fossil collection. An arctoceratid fauna occurs just above the Permian rocks, in a lithological setting similar to that Vikinghogda Formation occurring 2040m above the base at Hagrinden and about S0m above the base at Veidebreen Type Area: The Sassendalen Group is well- (figure 5 in Mark, Knarud et al. 1982). Peelina exposed at the mountains Vikinghagda and Sticky (1965, 1967, 1977, 1983) reported correctly that Keep in southern Sassendalen (Figs. 3, 4). The the basal Olenekian beds (the lower part of her lower part (Deltadalen Member) is well-exposed Wichebukta Formation) consist of fossil-poor, in the river banks in Deltadalen (type section of dark, laminated mudstone. Mark, Knarud et al. 1982), the valley between A short distance (12 km) further west, at Vikinghagda and Sticky Keep. The middle part Botneheia, Buchan et al. (1965) reported the basal (Lusitaniadalen Member) is exposed in the The Qpe section of the Vikingh@gdaFormation 55
southern foot of Vikinghagda. The upper part (ca. 80m) is better exposed in a mountain cliff ca. 1.5 km to the north-east (78“16’7N, 16”52’0E). The two sections can be correlated by following a pronounced bivalve rich dolomite bed at a level 173 m above the base of the formation (Fig. 4).
Thickness: The Vikinghagda Formation is 250 m thick in the type section. The thickness of the Deltadalen, Lusitaniadalen and Vendomdalen members are 68 m, 88 m and 94 m respectively. Buchan et al. (1965) reported the sum of these units to be 236m on northern Vikinghagda and 249 m at Sticky Keep. Mark, Knarud et al. (1982) reported 250m in the same section as studied here. At the western foot of Vikinghogda (Lusitaniadalen, Figs. 3, 5), the formation is estimated to be 266m thick, with the Deltadalen Member 67 m thick. The Vikinghagda Formation has its thickest development in this area and the equivalent units in western Spitsbergen are ca. 500 m thick (Mark, Knarud et al. 1982).
Equivalenfs: The Deltadalen Member is equiva- lent to the Vardebukta Formation in western Spitsbergen (Mark, Knarud et al. 1982), the lower part of the Urd Formation on Bjarnaya (Mark, Vigran & Hochuli 1990), and the Havert Forma- tion in the southwestern Barents Sea (Worsley et Fig. 3. Locality map. al. 1988). The Lusitaniadalen Member is equivalent to the Iskletten Member of the Tvillingodden Formation riverbanks of the tributary continuing around the in western Spitsbergen (Buchan et al. 1965; Mark, southern foot of Vikinghagda, informally called Knarud et al. 1982), and the lower part of the the Duboisbreen tributary. The basal Vendom- Sticky Keep MemberWichebukta Formation in dalen Member is well-exposed in the same the same area (Mark, Knarud et al. 1982; PEelina tributary and riverbanks, while the upper part of 1983). The Lusitaniadalen Member is also equiva- this member is best exposed in the surrounding lent to the middle part of the Urd Formation on mountain cliffs (Fig. 3).These river and mountain Bjornaya (Mork, Vigran & Hochuli 1990) and to cliff sections of the Vikinghagda Formation give the Klappmyss Formation in the south-western better exposures than the original type section Barents Sea (Worsley et al. 1988). (Buchan et al. 1965) on the northern part of The Vendomdalen Member is equivalent to the Vikinghagda which is partly scree covered, and Kaosfjellet Member (of the Tvillingodden Forma- the base is not exposed. These sections combined tion) and the upper part of the Wichebukta give a continuous exposure from the Permian Formation (Buchan et al. 1965; Mark, Knarud et Kapp Starostin Formation through the Viking- al. 1982; PEelina 1983). The Vendomdalen h@da Formation to the Middle Triassic Botneheia Member is also equivalent to the upper part of Formation which is found on both the Viking- the Urd Formation on Bjarnaya (Mark, Vigran & hagda and Sticky Keep mountains. Hochuli et al. 1990), the Klappmyss Formation in the south-western Barents Sea (Worsley et al. Type section: The base of the type section (Fig\. 1988) and the lowermost part of the Steinkobbe 3, 4) is located in Deltadalen (78 16’N, 16 53’E) Formation in the Svalis Dome (Mark & Elvebakk with the section following up-river around the 1999). 56 A. Mork et al.
Botr Fm. 120m
L /c Q) 0 9 A.b E 110 a, 2
/c 100 0 A.b
90
80
L a, 9 E Q) I I
c -a, m U m -c Q) n
@dB 0.b C.r 8.6 T.g A. W.
Perm Fig. -1. Vikinghogda Formation type section. The letters to the left of the lithology column indicate position and nature of rainples: P = Palynology. X = XRD, T = Thin-section. L = Lithology. Letters in italics are from the mountain section. See legend. 0 Ammonoids A. Anasibirites spp. A.b Arctoceras blomsfrandi Legend A.n Arctoprionites nodosus B. e Bajarunia ex gr. euomphala E.r Euflemingites romunderi Sandstone K. Keyser/ingites sp. K. s Keyserlingites subrobustus Siltstone 0. b Otoceras boreale P. 0 Popovifes occidentalis Shale PS Pseudosageceras sp. P'S Paranannites spathi Limestone S.S Svalbardiceras spitzbergense Tompophioceras cf. gracile Dolomite T. 9 W.f Wasatchites tardus Chert x.s Xenocelfites subevolutus Bivalves Nodule 0 A. Adontophora sp. Septarian nodule c.s Claraia stachei P.a Posidonia aranea Phosphate nodules P.m Posidonia mimer Calcite cement P. 0 Pseudomonotis occidentalis Gastropod Dolomite cement B B. b Bellerophon borealis Glauconite W. Worthenia sp. lntraformational conglomerate 77 Brachiopods R. Rhynchonellidae Erosional surface t Presence Planar lamination .G Last occurrence +L First occurrence irregular lamination Normal polarity Ripple lamination Reverse polarity Hummocky beddinghamination Not measured Fish remains
Vertebrate bones Magnetostrat. samples: river section, normal Increasing bioturbation . 0 river section, reverse Rhizocorallium 9 mountain section, normal mountain section, reverse Thalassinoides m mountain section, indeterm. 58 A. Mar-k et d.
Vikinghagda Formation dolomite beds and nodules are common. with few Lusitaniadalen silty interbeds. Calcite concretions are most abundant in the upper part of the Lusitaniadalen Member, but also occur with different carbonate mineralogy in other parts of the formation.
Deltadden Member The complete member is exposed in Deltadalen (68 m thick; Fig. 4). Lusitaniadalen (western side of Vikinghagda; Fig. 3) and on the flank of the southern hill of Stensiofjellet at its transition to Sassendalen. A development of more sandy (slightly thicker) beds transitional to the Varde- bukta Formation occurs at Bertilryggen on Oscar I1 Land. The upper part of the member is exposed in several sections in the outcrop area of the unit, and a more condensed development (without the earliest Triassic beds) occurs at Barents~yaand Edgegya. The uppermost part of the Kapp Starostin Formation and the basal sandstone of the Delta- dalen Member forms a cliff exposed on both sides of the Deltadalen River (Fig. 6A). It consists of2- 3 m of medium- to fine-grained glauconitic grey- green sandstone that occasionally shows faint cross-bedding. The sandstone is moderately bio- turbated and has a patchy chert cement. Tlzalassi- noides trace fossils are often filled by chert nodules. The top of the Kapp Starostin Formation is fractured and cherty with an irregular brownish- weathering coloured surface. The base of the Deltadalen Member is defined at this weathering surface (Figs. 6A, B, C). which is irregular and has
~~~ ~ Fig. 6. Photos from the type section. A) Triassic glauconitic sandstone rest5 sharply on cherty Permian aandstone. Measure rod is one metre long. B) Details of the PermianTriaasic boundary beds. Note erosion surface with gutter cast at boundary. C) Basal Triassic sandstone. Note drillholes for rnagnetostratigrdphy sainplea at base and top of bed. D) Sandstone interval between 12 and 14 m. The fossiliferous Fig. 5. Lu5itaniadalen \ection. Legend with Fig. 4. nodule with Oforeras boreole was located at the level of the geologist. E) Planar bedded thick sandstonelsiltstone beds (17- 13 ni) iii the lower pan of Deltridalen Member. F) Thin sandstone beds in the upper part of the Deltadnlen Member Lirhology: The formation is dominated by silty and the boundary at 68 in to the overlying silty mudstone of the shale. In the lower part of the Deltadalen Member Lusitaniadalen Member, however with one thin sandstone bed sandstone and siltstone interbeds are abundant; (68.6 in) in the lowermost pan. G) Detail of 6F. H) The silty siltstone and very fine-grained sandstone inter- mudstone in the lower part of the Lusitaniadalen Member. Note marker horizons at 97.6 m. the flattened globular nodules at beds are less common in the Lusitaniadalen 95 111, and rhe double siltstone bed at 100 ni which also appedrs Member; whereas in the Vendomdalen Member in Fig. 7A. 1) Detail of 6H. The type sectioti of the Vikitighpgda Fortnution 59 60 A. Mdrk et a]. small channels (gutter casts?) that are filled by sandstone bed. indicates rapid establishment of medium-grained sandstone. The surface also conditions favourable for benthic colonization. contains irregularly shaped pits and grooves The repeated occurrences of siltstone and (maximum 7 cm deep and 8 cm wide) producing sandstone beds with hummocky lamination in- an angular shaped surface, resembling a karstic dicates storm influence on a shelf above storm erosion surface. A thoroughly burrowed, greenish- wave base. Sediment supplied from the deltaic grey, fine-grained sandstone (1.2 m thick), coar- coast in the west (Mgrk, Knarud et al. 1982) may sening-up to medium-grained in the upper parts, have been built up above storm wave base, where rests on the erosion surface (Figs. 6B, C). Some sheet sand bodies were laterally spread out on the chert clasts of the underlying lithology occur in sea floor. This model is consistent with the this sandstone which splits into 10-30cm thick distance of approximately 75 km to the coastal beds. sequence present on the west coast of Spitsbergen, Above the basal sandstone, the Deltadalen and the more distal. basinal shelf sediments further Member consists of silty shale with intervals east on Spitsbergen and EdgeGya. dominated by siltstone or very fine-grained sandstone beds. Between 12 m and 14 m (Fig. 4) Liisittirziadalen Mrniher thickly bedded siltstones form a unit (Figs. 6D, E) which has a base containing calcareous nodules The unit is named after a valley on the northern with a rich fauna of the Otoceras boreale Zone. side of Vikinghagda (Fig. 3). The type section is Several intervals enriched in sandy siltstone beds well-exposed in the Duboisbreen tributary at the occur throughout the member, and several show foot of Vikingh~gda(88 m thick; Figs. 3, 4). In hummocky lamination, the upper parts of which other areas the transition from the underlying are often rippled. Bioturbation is sparse. Calcite Deltadalen Member is often covered in scree. concretions (up to 30cm in diameter) occur at a The base is defined where dark grey laminated few levels higher in the member. silty mudstone sharply overlies the hummocky The top of the member consists of thin laminated sandstone at the top of the Deltadalen sandstone beds forming an upward-coarsening Member (Figs. 4, 6F). This transition may give a sequence (Figs. 6F, G). This part of the member break in slope which can be recognized in areas of is well-exposed on the southern side of the poor exposure. Duboisbreen tributary near its junction with the The lower part of the member is exposed on the Deltadalen river. There is a minor gap in the southern side of the Duboisbreen tributary (Fig. section at the river junction creating some 6F), while the remainder can be studied on the uncertainties in section correlation and thickness. northern banks (Fig. 6H). There may be some The thickness of the member and the sandy minor uncertainties in correlations within this uppermost beds are quite similar to the develop- member partly due to scree cover. The upper part ment seen in Lusitaniadalen on the western side of of the member is well-exposed in a small canyon Vikinghagda (Fig. 5). on the mountain side (Figs. 7A, B). Most of the mudstone is finely laminated and Depositional environments: The weathering crust only sparse bioturbation is observed. The lower on the erosional surface at the base of the section part is dominated by dark grey silty laminated indicates exposure of the top of the Permian Kapp mudstone. Some metres above the base sandstone Starostin Formation, prior to deposition of the Deltadalen Member. A similar erosion surface is reported from Edgeaya (Mgrk, Knarud et al. 1982). At the equivalent boundary in Lusitania- Fig. 7. A) The middle and upper part of the Lusitaniadalen dalen there is no erosion, but a yellow-weathering Member. Level 100 m from Fig. 6H is indicated. Fig. 7B and C .;how detail of parts of this photo. B) Detail of A showing the bed occurs at the boundary. Above the erosional upper part of the Lusitaniadalen Member. The boundary with surface. the basal beds contain fragments and the Vendoindaleri member is at 156 m. C) Shaly nodular interval debris of the underlying lithologies and palyno- high in the Lusitaniadalen Mh. D) The bliae of the Vendomdalen morphs (see below) related to those of the Kapp Member is defined on top of the yellow weathering silty Starostin Formation. The extensive bioturbation, dolomite bed. The top of the section is represented by the bivalve-rich regional marker bed at 173 m. E) The upper part of including ThalasJinoides as a deep tier (cf. the Vendomdalen Member on the eastern slopes of Viking- Bromley & Ekdale 1986) in the transgressive hogda. The light-coloured levels represent dolomitic hedh. The rye section of the Vi!iingh@gduFoiniatiorr 6 1 62 A. Mdrk et 01. beds occur, arranged in faint coarsening-up lower boundary, and the yellow weathering sequences. Some of these display hummocky dolomite beds are distinctive of the Vendomdalen lamination and cross lamination. Small (20- Member throughout central Spitsbergen. The 30 cm in diameter) globular or flattened carbonate dolomitic beds may be up to 1.5 m thick, but most nodules occur in a few horizons from ca. 15 m are 10-30 cm thick. Dolomitic nodules, some of above the base of the member (Fig. 61). and a them septarian, are up to tens of centimetres in prominent horizon of large septarian concretions is diameter; flattened nodules may reach several found 25 m above the base. Calcite concretions are metres in horizontal extent but generally only abundant in the middle and upper parts of the 0.5 m in thickness. Rare calcite concretions occur member (Fig. 7C). These concretions formed early near the top of the member. in diagenesis, as is evident by deformation of the The type section continues ca. 1.5 km to the enclosing shales, and the fact that the enclosed north-east where exposures from the bivalve bed fossils are not crushed. Abundant ammonoids and (at 173 m; Fig. 4) upwards occur at ridges between bivalves occur in a calcareous lens (154 m; Fig. 4) melt water creeks. This section consists of several close to the top of the member. The Lusitaniada- 3 to 12 m thick, faintly coarsening upward units, len-Vendonidalen member boundary is placed at grading from laminated shale to silty mudstone, the top of a dolomite cemented sandstone (Fig. capped with dolomite beds, sometimes silty or 7D). sandy, or consisting of dolomite lenses. The Fossils occur throughout the member, except dolomite beds consist of sucrose, ferrous dolomite the lower 30 m, and are mostly concentrated in (from SEM/microprobe analyses) and were concretions. Ammonoids dominate, but bivalves formed relatively late in diagenesis. The upper are also common. often as imprints in sandstone/ 50 m consist of planar laminated silty grey carbonate beds. Several levels with vertebrate mudstone with thin dolomite beds. At the top is a remains are recognized. pronounced silty/sandy dolomite bed with abun- dant, though poorly preserved imprints of ammo- Depositional einirontnents: The lower part re- noids. The bed shows some ripple lamination. presents a transgressive development from the Above the top bed, very dark grey shale with underlying member towards a distal shelf envir- small phosphate nodules is referred to the onment. The overall setting represents moderately Botneheia Formation. Seven metres above the deep shelf deposition. distal to the deltaic input base of the Botneheia Formation there is a from the west. dolomitic siltstone bed, bioturbated by Rhizocor- alliuin. This bed represents a local marker in the lowermost part of this formation in the Sassenda- Vendotiidden Member len area. The Vendomdalen Member (94 m thick) is named after a valley IS km south-east of Vikingh~gda Depositional environments: The member repre- where it is well-exposed in the surrounding sents distal shelf deposits, below wave base, with mountain sides. The lower part of the type section accumulation of marine derived organic material is defined at the southern foot of Vikinghagda in a low oxic environment. where the basal beds are well-exposed (Figs. 3. 4. 7D). The major part of the member (and the upper boundary) is exposed in all outcropping areas of the Vikinghogda Formation. The type section Palaeontology (except the basal beds) is defined on the eastern slope of Vikinghagda (Figs. 3, 4, 7E). The two Macrofossils which can be identified (Fig. 8) are sections are correlated at a prominent bivalve-rich restricted almost exclusively to concretions. dolomite bed 18 m above the base of the member Shales between the fossiliferous concretion-levels at 173 m (Figs. 4, 7D). are either not fossiliferous or have only indetermi- The member consists of silty. dark grey, nate fauna, so detailed ammonoid zones or laminated mudstone, thin- to medium-bedded. distinctive biostratigraphical boundaries, cannot with more or less silty. yellow weathering. easily be defined. The fauna of a single concretion- dolomite beds and nodules. A clear shift from layer represents a snapshot of the zone or higher grey to dark grey mudstone takes place at the biostratigraphical unit, consequently only compar- The hpe section oj thr Vikirigh@gdaForn~ntion 63 ison with ammonoid assemblages from other more 1989). Some fragments also resemble M. bitteri. fossiliferous boreal Triassic successions, such as in which has a younger range (Wordian-Capitanian; Siberia and the Canadian Arctic (Weitschat & see discussion in Henderson 1997). These con- Dagys 1989: Dagys & Weitschat 1993) allows a odonts provide no conclusive age for the sampled more precise biostratigraphical interpretation. level. A similar fauna of Mesogoiidolrllu also One sample from the Kapp Starostin Formation occurs at the transition between the glauconitic and five samples from the lower part of the sandstone and dark, soft shales, i.e. 0.5 m above Deltadalen Member have allowed recovery of the base of the section. conodonts. A single sample from a calcareous The samples at 5.0 m and 11.5 m contain nodule was processed for conodonts using stan- preserved elements of Neogoridolella carinntci. dard acetic acid technique. The remaining samples The 1 1.5 m sample also contains large numbers of were taken from moderately lithified sandstones phosphatized gastropods and bivalves. while the and shales and processed using a "freezing and sample at 47.0m only contains a single broken thawing" technique (Pojeta & Balanc 1989). All ramiform element. The sample at 69.0ni (top of samples produced small numbers of conodonts. the Deltadalen Member) contains a single element of Neospathodiis cf. si~albarderisis,and indetermi- nate Neogoridolella sp. Deltaduleri Member The biostratigraphical control on this unit is poor. Disciissioti: Conodont faunas from the Lower A single fossiliferous horizon occurs in the type Griesbachian Otoceras concavum and 0. boreale section in a layer of carbonate concretions 1 1 .S m zones are generally sparse in the Boreal Triassic. above the base of the member (Fig. 4). with the From the type section at Griesbach Creek (Arctic following fauna: ammonoids Otocerus borcwle Canada) only a few indeterminate conodont Spath (quite large. badly preserved specimens), fragments have been recovered from the 0. Tonzpopl~icer~iscf. grurilr (Spath): bivalves Clar- concavum Zone (Orchard & Tozer 1997a, uici .stcrchei Bittner, Adontophora sp.; gastropods 1997b). From the Boreal lower Griesbachian Bellerophon borealis Spath, Worthenia sp.; bra- succession (Siberia, Svalbard) several Nrogondo- chiopods Rhynchonellidae. The co-occurrence of lelln species have been reported from strata below 0. bore& and ophiceratids indicates that this the 0. boreale Zone (Dagis 1984: Dagis & level represents the upper part of the Otoceras Kortinskaja 1987). Of the index species proposed boreale Zone. 0. boreule has also been described by Yin et al. (1988) for the base of the Triassic, from the adjacent Lusitaniadalen (KorEinskaja lsnrcicella panw (= Hinclrorliis yanw). only a 1986). single sample has been described from the Throughout Svalbard there are few Induan strata lowermost Triassic of western Canada (Henderson with additional ammonoid-bearing horizons. From 1993). These beds occur below the 0. boreale the upper part of the Griesbachian and the lower Zone, but the lack of the index ammonoid 0. part of the Dienerian, KorEinskaja ( 1986) has c'oiz~*m~mhampers the biostratigraphical correla- found, Proptychites cf. strigatus and P. rosen- tion. kmntzi from both Lusitaniadalen and Dickson Following the paper by Yin et al. (1988) many Land. From the upper Dienerian Vuviloiites aff. conodont studies have focused on the Perniian- sivrdmpi was recorded from the Bellsund area Triassic boundary beds (Dickins 1977; Kozur (Gazdzicki & Trammer 1977) and Va\iloiitcs 1989. 1995: Zhang et al. 1995; Kozur et al. spitsbergensis from Van Keulenfjorden and Lusi- 1996: Lai 1997; Orchard & Tozer 1997a, 1997b: taniandalen (Kortinskaja 1986). V. spitshargrri.sis Yin 1997). However, the conodont occurrences in also occurs at Bertilryggen (Oscar I1 Land) about the basal Triassic beds are still not well under- 40m above the base of the Triassic (W. stood, and the absence of Isarcicrllu panw in the Weitschat's observation). lowermost part of the Deltadalen Member may Conodonts from 5 in below the base of the have several reasons: section show IS fragmented Pa-elements of Mesogondolella resembling M. iduhoerisis, pre- 1) I. piiwa may not have been adapted to cool viously described from Spitsbergen by Szaniawski Boreal water temperatures. & Malkowski (1979) and the Assistance Forma- 2) The transgression at the base of the Deltadalen tion of the Sverdrup Basin (Beauchamp et al. Member was rapid and the conditions may have 64 A. M@rk Ct al. Tlir vpe section qf the Vikinghggdo Formation 65 been too deep for Isarcicellu (Hirideodiis), which Liisitariiudalrn Member Henderson ( 1997) regards as a near shore euryha- line form in contrast to the more open marine form Except in the lowermost 30 m, fossils are common Neogondolrlla . in the type section. Due to the abundance of early- 3) At present it is not proven that sedimentation formed calcite concretions. the higher part is the during the lowermost part of the Deltad:ilzn only unit within the Svalbard Triassic in which it is Member is continuous. possible to separate faunal zones based on the 4) Sampling may have been too sparse. ranges of ammonoids. This horizon was formerly known as the "Fish-Niveau" from which Stensio The lack of I. pnn~ci in Svalbard may thus be a (1921, 1925) described a rich fish fauna. facies or climatic effect as reported in Canada by The lowest fossiliferous level (98 m: Fig. 4) Henderson ( 1997), similar to the general absence contains only large arctoceratids which indicate of Hindeodirs in the Permian of Bjarnraya (Nakrem the Euflemingites romunderi Zone of the Smithian 1991). The general absence of I. ptvuin Boreal Substage. The index ammonoid EiijZetningites areas may thus indicate that the selection of this ronirrridrri is quite rare and has its first occurrence fossil may not be the best choice for defining the in the type section at 128 m (Fig. 4), in a grey global PiT-boundary. mudstone with numerous levels of nodules which Neogondonrllo cnriiiata is well-known from contain a rich ammonoid and bivalve fauna. lowertnost Triassic sections in western Canada Ammonoids from the E. romunderi Zone, apart (Henderson 1997), where a range through most of from the index-species, are: Arctoceras blotti- the Griesbachian is recorded. N. curinata has been straridi (Oeberg), Puratiunnites spathi (Frebold) previously recorded from Spitsbergen in associa- and Anukashniirifrs sp. The bivalve Posidonici tion with Otocercis (Dagis & Korcinskaja 1987). riiirner is also characteristic of this zone and occurs Neospatlrocirts svulbardensis as reported from in the type section at several levels. In the type southern Spitsbergen (Birkenmajer & Trammer section the highest ammonoids from the E. 1975; Nakrem & Mark 1991) is also known from romunderi Zone occur at 152 m (Fig. 4). the type locality of Diener Creek in Arctic Canada Ammonoids from the carbonate nodule layer (Orchard & Tozer 1997b) and indicates the above 152 m (at 154.5 m; Fig. 4) indicate the Protychites candidus Zone of early Dienerian kige. Upper Smithian Wasatchites tardus Zone, which extends upwards from this level. This zone is characterized by a typical prionitid ammonoid fauna (Frebold 1930; Spath 1934). This zone is Fig. 8. Ammonoids from the Vikinghagda Formation type scction. A) Tonzpophicerus cf. gnirik (Spath). Grieshacl1i;in. known from all sections in central Spitsbergen Otoceras hore;tle Zone. Deltadalen Member. I1.5 ni ahwe TIP (Dickson Land, Oscar I1 Land, Sassendalen area), boundary; Deltadnlen, Spitsbergen, x2. BI Eidlcnibigirt..\ the east coast of Spitsbergen, Barentsaya and nvmozderi Tozer. Smithian, Euflemingites romunderi Zone: Edgeaya. The fauna collected from the type Vikinghagda Formation. Lusitaniadalen Member, I78 in ahore section contains the following species: Wusatch- PiT boundary: Duboisbreen tributary. C) .4rcrocerirs h/orri.\rrc~~t- di toeberg), Smithian. Euflemingite\ romunderi Zone; Vikin- ites tunhis (McLearn), Xenoce1tite.r ~iibevoliitus ghpgda Formation. Lusitaniadalen Member, 1 I2 ni ahow P/T (Spath), Arctoprionitrs nodosiis (Frebold). Anasi- boundary; Duhoisbreen tributary. D) Porcmimiiros spdii birites spp. and Pseudosngecrnis sp. The bivalve tfrebold), Sniithian, Euflemingites romunderi Zone: Viking- Pseudotnonotis occidentulis (Whiteaves) is also hggda Formation. Lusitaniadalen Member, I37 m abovc P/T characteristic of this level and known from bouiidary; Duboisbreen tributary. E) Xmoceltires suhridririrt (Spnth). Srnithian. WasatchiteL tardus Zone; Vikinghopda contemporaneous beds in the Canadian Arctic. Formation. Lu.;itnniadalen Member, 1.54.5 m above PiT bound- The septarian carbonate nodular layer at 155 m ary: Duboisbreen tributary. F) Wusririhires riirdirs (McLem), contains, besides ammonoids, quite well-pre- Smithian, Wasatchitea tardus Zone; Vikinghagda Fwmation, served skulls of stegocephalian amphibians (Wi- Lusit:iniadaleii Member, 151.5 in abo1.e P/T boundary: Du- boicbreen tributary. C) S~~n/kin/ic~~,~clr.qiichcvgemr Frehold. tnan 1910, 1916. 1933). In the boundary beds of Lipper Spathian, Kryserlingites subrobustus Zone; Vikinghogda the Lusitaniadalen Member and the Vendomdalen Formation, Vendomdalen Member: 9 m below top of the Member Xenoceltites siibr\dutus is present. formation; Vikingh~gda mountain cliff. H) Kener/iuqif~\ indicating the W. tardus Zone. This implies that .siih,rihusrsirs (Mojsisovicsl, Upper Spathian. Keyserlingiteh subrobustus Zone: Vikinghggda Formation, VendoniJ;ileti the transition to the Vendomdalen Member Memher; 9 m below top of the formation: Vikirigh@a probably takes place within the Upper Smithian mountain cliff. W. tardus Zone. 66 A. Mq~ket ul.
Veiidonidulen Menzber changes in the morphological textures probably took place during early diagenesis with precipita- Within this member carbonate concretions are rare tion of pyrite (framboids and individual crystals) and mainly restricted to the uppermost part of the and recrystallization of carbonate. unit. Most of the fossils in the dolomite beds and The kerogen log is based on particle counts, concretions are compressed and poorly preserved. recognizing different stages of degraded woody hampering exact determination. material and palynomorphs. Plankton. pollen and At 173 m (Fig. 4) a prominent dolomite bed spores were counted individually where preserva- contains abundant bivalves and some ammonoid tion allowed. The categories were grouped for imprints. These ammonoids have been compared kerogen description and an extra group was added with material from Siberia, and they belong to for homogenized sheets or flakes. The counting Bajarunia ex gr. euoniphala (Keyserling 1845) was carried out preferably on sieved residues, but indicating the Bajarunia euomphala Zone of the also on slides from further stages of chemical lowermost Spathian. processing. This was necessary to remove pyrite or In the type section. a Spathian age is clearly to disintegrate the dense aggregates found in demonstrated by the presence of the ammonoid organic rich samples. The degraded woody Keyerlirigites sp. upwards from ca. 219 m (Fig. particles are clearly affected by the oxidative 4). In the boreal Spathian ammonoid zonation the treatment and therefore under-represented in many genus Keyserliiigites is restricted to the latest Late samples. The continued processing and sieving Spathian zone (Dagys & Weitschat 1993). also cause large fragments to break into smaller The carbonate nodule layer at ca. 241 m (Fig. 4) pieces. Finely dispersed amorphous/degraded ma- contains a well-preserved latest Spathian fauna terial has been evaluated as a percentage of the (Weitschat & Dagys 1989) which in the type total residue and removed from the counting. The section. includes: Keyserlingites strbrobustrrs distribution chart for Vikinghagda (Fig. I1) shows (Mojsisovics), Svulbardicerus spit:bergetzse (Fre- that there are few age diagnostic fossils and they bold) and Popovites occidentdis (Tozer). The have only scattered appearances. bivalve Posidotiia arai~e~(Tozer), which is restricted to the Keyserlingites subrobustus Zone of the Boreal Triassic, also occurs at this level. Field work at Milne Edwardsfjellet (about Kupp Starostiri Fonnutioii 15 km south-east of the type section) has produced One sample from 5 m below the top of the Kapp additional biostratigraphical information concern- Starostin Formation yielded a residue with abun- ing the Vendomdalen Member. From a dolomite dant woody material. The palynological assem- nodule layer about 16 m above the “bivalve bed” blage comprises common Vitrutinu spp. besides (ca. 34m above the base of the member) the Apiculutisporis laiijouwii, Crebesporu conceiitri- ammonoid Parasibirites cf. elegarzs (Dagys & cu. Kraeuselisporites cipicirlatus, K. spitiosirs, Ermakova 1988) was collected. This species is Liieckisporites virkkiae, Neoraistrickia spp.. Pro- known from the upper Spathian of Siberia (Dagys tohaploxypiizus perjectus, P. sunioilo,ichii and & Ermakova 1988). indicating correlation to the Vesicaspnrci spp. The plankton comprises abun- Parasibirites grambergi Zone. Transferring this dant Cpatiospkuem besides Filisplmeridiirnz information to the type section indicates that the setmessitante, Micrhystridi~inispp. and Unelliiiin uppermost ca. 60 m are of Late Spathian age. spp. The assemblage correlates with the Scutas- porites cf. unicus-Lunatisporites spp. Assemblage. described by Mangerud (1994) from the upper- Pal y nolog y most part of the Tempelfjorden Group on the Finnmark Platform. The equivalent kaeuselispor- The acid insoluble remains from the Vikinghogda ites Assemblage documented from Svalbard type sections are generally badly preserved. The (Mangerud & Konieczny 1991) regularly contains kerogen log (Fig. 9) shows that indeterminate the same plankton. palynodebris. often homogenized as sheets or flakes, dominates (Fig. 10). The original morphol- ogy is poorly defined and mostly allows identifi- cation only to major palynomorph groups. The Fig. 9. Palynofiicies. TOC and RockEvnl data. The rype section of the Vikinghgjgdu Formation 67 68 A. Mmr-k et (11. The type section of the Vikinghbgdn Fortnutiori 69
Deltcickt lei 1 MernOr I' which the index fossil T. sroschicina is sparsely represented (Mangerud & Konieczny 1993). There The organic residues from 0.2-1.7 m. representing is no sign of an acme zone for this taxon; on the the basal sandstone of the Deltadalen Member, are contrary the published evidence indicates that T. rich in woody material. Permian palynomorphs are stoschianu is more regularly represented towards relatively abundant (Fig. 11), represented by the upper part of its range. The palynology of the LueciYsporitrs virkkiae, Vitratinii spp. and plank- Vardebukta Formation. (apart from the base) has ton. comprising Cyniurio.~pI~urrci.Fi1is~)haeriilicrtii so far not been documented, and it is not known if setiisessitunr~~.Mi[.r~iysrri(liiiin and Uiielliuni spp. Assemblage P is restricted to the Griesbachian in The assemblage is reminiscent of that from the Svalbard. On the Finnmark Platform, Barents Sea. Kapp Starostin Formation below. Mangerud the Lundbladispora obsoleta-Tympanicysta (1994) described similar features from layers ,just stoschiana Assemblage is recorded throughout below the base of the Havert Formation on the the lowest part of the Havert Formation. Here. Finnmark Platfomi. the diverse assemblage comprises T. stoscl~iunn The organic residues from 4.7-14.0 ni above the and other fungal remains (Mangerud 1994). base of the Deltadalen Member are dominated by Equivalent assemblages from Greenland and the variably degraded palynomorphs. Fili.spkuo~i- Canadian Arctic occur in the three lowest diunz, Micrliystritli~~tn,Densoisporites iwjbiirgii Griesbachian ammonoid zones (Balme 1980; and Lii.tintisporites spp. dominate the palynologi- Piasecki 1984; Utting 1985. 1989). cal assemblage. Crustaesporites GrobP- glohosus. Organic residues from 20.348.0 m above the spom cmcentricn. Lueckisporites lirkkirie. base of the Deltadalen Member comprise abun- Mucirltirnst?oritrs spp., Proprisporites p(icockii dant plankton, pollen and spores and their and Uiuesporites irnperialis represent subordinate degraded products. The mainly indeterminate age diagnostic forms (Figs. 10. 12). The strati- palynomorphs have walls damaged by mineral graphically significant ~wpanicy.rtastoschimu is growth (pyrite). Micrlzvstridiuin and F. setiisessi- recorded as rare at the top of the interval. The tame. D. nejburgii. Cjcndopires nitidus, Lutiatis- assemblage is correlated to the equivalent Lund- porites spp. and Prrtricol~?ipallt.Ilirrs spp. bladispora obsoleta-Tympanicysta stoschiana As- dominate the palynological assemblage (Fig. 1 1) semblage Zone of Mangerud (1994) and to and represent the basic elements also recovered Assemblage P of Hochuli et al. (1989). from Assemblage 0 of Hochuli et al. (1989). In Svalbard. Assemblage P is reported from the Distinguishing features for this interval are the basal layers of the Vardebukta Formation. in association of Arntrisporites spp., Bharuchrujis- porn ltihiclzensis, Cordnitina minor, Densoispor- ites cornplicutus, Kraeuselisporites apiculatirs, K. hoofddijkensis, Lueckisporites virkkiae. Pechnr- Fig. 10. Palynofncie\ and palynomorpha from Vikingh(4gda osporites coronntus, P. inter-inedius and Propri- Formation. Deltadnlen. The metre level ia followed by a letter sporires pocockii. Maculcitasporites sp. seems to code indicating progresaive oxidation levels (XI-XS: SI = - \ieved residue) and slide coordinates. The exposurea are throngh be missing from the assemblage, but has been x40 lenses. unless otherwise indicated. A) Palynofacies from correlated to Svalisl that has been recovered from the Deltndalen Member. 67 m, XI. 99.2-33.1 (~2.5).Pyrite the Ophiceras commune Zone of the Svalis Dome damage. B) Palynofxies from the Lusitaniadalen Member. (Vigran et al. 1998). Although the index fossil T. 141.2 m, Si. 103.2-33.5. Sheetslplates. C) Palynofacies lrom the Venilomdalrn Member. I bR in. X2. 94.8-35. I. RL~II~~I~.\/IO~~Istoschiutzii is missing, the assemblage is consid- ,j%iw/cifu. D) "Fungal remains'.. a bent tube with partition Irm ered as equivalent to Assemblage P of Hochuli et Lusitaniadalen Member, 137.5 m. Si. 100.6-26.4. E) CV?I~~ The ~prsectiori of the Vikirighlgda Formation 13 degraded aggregates obscuring the embedded mation and a characteristic pattern for the palynomorphs. The dominant palynomorphs are individual members. Micrhystridiurn and Tasnianites and bisaccate In the Deltadalen Member low TOC values pollen, in particular those from the Striatoabieitrs (mostly Table I. Organic richness (TOCJ and RockEva1 pyrolysis data. Level TOC Rock-Eva1 Pyrolysis Hydrogen Production rn B. s1 s2 Tmax ‘C index index 250.50 1 .oo 2.14 2.49 439 249 0.46 249.30 0.57 - - - - - 246.70 4.4 1 2.81 14.67 442 333 0.16 242.30 3.73 3.18 12.84 439 344 0.20 233.80 1.55 1.23 4.03 428 260 0.23 226.00 1.95 - - - - 22 1.80 2.76 1.63 8.89 40 322 0.15 213.00 1.86 I .85 4.72 439 254 0.28 200.40 1.90 I .40 4.53 439 2389 0.24 190.30 1.62 - - - - 188.50 2.69 I .63 7.71 442 287 0.17 184.00 1.06 - - - - 177.70 2.28 1.59 6.47 44 1 284 0.20 173.60 0.91 - - - - 172.00 2.26 1 .I6 6.5 I 442 288 0.21 169.00 3.04 4.83 10.80 445 355 0.3 I 168.00 1.34 - - - - 164.50 2.78 3.26 9.33 443 336 0.26 159.00 2.23 2.24 6.29 44 1 282 0.26 156.80 1.23 155.80 I .96 I .61 5.5 1 444 28 1 0.23 155.50 0.84 - - - - 150.50 1.12 0.98 2.14 442 191 0.3 I 146.70 0.54 144.20 I .02 - - - - - 143.20 1.27 I .39 2.15 440 169 0.39 138.90 0.55 0.52 0.65 439 118 0.44 128.20 0.75 0.56 1.01 438 135 0.36 122.30 0.78 0.86 1.16 437 149 0.43 102.30 0.26 - - - - 101.00 0.60 0.36 0.76 438 I27 0.32 95.00 0.66 0.59 1.29 437 195 0.31 89.00 0.58 0.7 1 1.11 436 191 0.39 87.00 0.66 - - - - 84.00 0.59 0.58 0.90 439 153 0.39 75.80 0.54 0.3 1 0.79 438 146 0.28 70.80 0.30 - - - 68.60 0.54 0.32 0.69 439 128 0.32 67.80 0.476 67.00 0.24 65.80 0.21 - - 62.20 0.3 I 35 0.58 56.60 0.22 - 37.00 0.56 200 0.54 27.50 0.28 - - 20.30 0.24 14.00 0.29 13.80 0.47 - I 1.20 0.27 - - - - - 7.60 I .oo I .ox 1.68 438 168 0.39 4.70 1.78 2.49 4.33 444 243 0.37 1.10 0.26 - - - - 0.20 0.33 The type .section of the Vikingh@gdaFonnation 75 et al. 1993: M~rk& Elvebakk 1999), showing that The two horizons sampled from the Kapp the transition to environments with improved Starostin Formation (Fig. 4) show reversed preservation potential of organic material is ii polarity. This could indicate either a youngest regional phenomena. Tatarian age, or a somewhat older age in the late The RockEval T,,,, values vary between 436 Permian (Gialanella et al. 1997). The long normal and 445"C, and the values are similar to those polarity magnetozone (Vln) at the base of the reported by MGrk & Bjoray (1984) from the Deltadalen Member is probably the GNI magne- Middle Triassic succession of the same area, tozone of Ogg & Steiner (1991), which has been indicating that the whole succession lies within identified in sequences in Asia and Europe (Haag the oil window. The production index is mostly & Heller 1991; Steiner et al. 1993; Nawrocki low, but several samples have values between 0.3 1997) and characterizes the boreal lower Griesba- and 0.6, indicating that some hydrocarbon staining chian ammonoid zones. In addition, within GNI, has occurred in the succession. short reversed polarity magnetozones have been found in the Siberian traps (Gurevitch et al. 1995) and in China (Haag & Heller 1991). which may correlate to the short reversed intervals at 1.8 m, Magnetostratigraphy 10 m, and 13.3-14.8 m (Fig. 4). It is unclear, because of a sampling gap at the base of the Samples for magnetostratigraphy were collected Deltadalen succession, if the normal polarity mostly from siltstone and sandstone beds in the continues through the basal transgressive shale of Deltadalen and lower Lusitaniadalen members, the Deltadalen Member. and from concretionary calcite and dolomite in the The top part of the Deltadalen, and lower part of Vendomdalen Member and the upper part of the the Lusitaniadalen members (36-105 m; Fig. 4) Lusitaniadalen Member. The samples were sub- contain reversed and normal polarity magneto- jected to conventional thermal and alternating zones. The overall mixed polarity character of this field (AF) demagnetization to isolate the char- interval is the same as the mid Griesbachian to acteristic remanence. Thermal demagnetization to lower Smithian of Ogg & Steiner (1 99 1) and Haag 250 'C, followed by AF demagnetization to 80 mT, & Heller (1991), and less well-dated European proved effective in removing a present day-like sections (Nawrocki 1997). The overall mixed overprint from the Triassic magnetization. The polarity of this interval indicates that most of the magnetization appears to be carried by a combina- Dienerian and lower Smithian is probably present. tion of magnetite and magnetic sulphide. The If this were not so, more normal polarity would be palaeomagnetic details will be presented else- evident in the upper parts of the Deltadalen and where. lower parts of the Lusitaniadalen members. Stratigraphic height details differ slightly from Over the interval 36-105 m the following those presented in Hounslow et al. (1996). because correlations to the Ogg & Steiner (1991) results of stratigraphical re-evaluation made during field- from the Sverdrup Basin are the most plausible: work in 1997. The magnetozones have been numbered into reversed-normal polarity couplets. I) Vlr.nl is the equivalent of GN2 of the Sverdrup in the same way as marine magnetic anomalies are Basin study. In the Sverdrup Basin GN2 is a thin referenced (Cande & Kent 1992; Kent et al. 1995). normal zone, found only at the Creek of Embry The prefix V refers to the Vikinghagda section. locality. GN2 is late Griesbachian, based on Using such a scheme the normal magnetozone ammonoid control. V2n at 55 m (Fig. 13) is composed of sub- 2) V2n is equivalent to DN 1. which was identified magnetozones in descending order V2n.n 1 (nor- at the Creek of Embry and Griesbach Creek and is mal), V2n.rl (reversed) and V2n.112. The work of a relatively thick normal polarity zone. like V2n Ogg & Steiner (1991) provides the most closely from the Vikinghagda section. From the Sverdrup comparable Lower Triassic magnetostratigraphic Basin study DN1 is early Dienerian. study. In their study of the Sverdrup Basin 3) VSn and V5r.nl are equivalent to SMN1. Both sequences. magnetozones were numbered with at Vikingh~gdaand in the Sverdrup Basin study, codes GN, DN and SMN indicating normal these polarity zones correspond to the basal part of polarity zones in the Griesbachian, Dienerian und the E. romunderi Zone. Smithian respectively. 4) V3n and V4n correlate with the interval 16 A. M@rk et al. Amrnonoid west Unit Lithology zone P*rpel 1 unk - t Botneheia QY 4nisian #w Darkphosphatic % Iu Rhizowrallium bed Fm. shale 05 -250 Svalbardiceras - spitzbegense Keysedigites Keysedingites sp. Subrobutus Keysedingites sp. ______ 'Parasibrites grambergi I ______ Bajarunia Bivalve bed euomphala Xenoceltites _7--1- su&wl~us lasakhiteJ tardi Start W.tardusZm +- Arclaceras Iblomstmdi Euflemingites romunderi -Arcto~~as bfomstrandi E LL U I- Y 3 m W D a - Otoceras boreale Otoceras a boreale > WPP PERMIAN Starostir -Fm. * From data from Milne Edwardsfiellet 1. Weitschat 6 Dagys I9 2. Hcchuli el a1.191 md Wgran el al Intetprete Fig. 13. Summary diagram from the type aection. Legend with Fig. 4 The type section of the Vikinghggda Fonnation 77 between DNI and SMNI. In the Sverdrup Basin, Edwardsfjellet 15 km further south-east displays the section with the largest sedimentation rate over the same remagnetization. this interval was Embry Creek. This section possessed two normal polarity zones between DN 1 and SMN I over this interval (DN2 and a lower unnumbered normal polarity zone). V4n Discussion may correlate with the upper (DN2), and V3n with the unnumbered lower magnetozone from Embry Using a multidisciplinary approach to establish Creek. Biostratigraphic confirmation of the age of this new type section highlights the dangers of these magnetozones from the Sverdrup Basin was erecting type sections based on restricted informa- lacking, but they may occur in an interval between tion. Although the conceptual definitions by the upper Dienerian and lowest Smithian. Buchan et al. (1965) and Mgrk, Knarud et al. (1982) are still valid, wrong correlations to other These correlations would place the age of the top areas (i.e. western Svalbard), resulted from poor of the Deltadalen Member as mid-Dienerian. This exposures in the previously defined type section, is compatible with the Griesbachian-Dienerian and the erection of succeeding type sections in palynology age of the upper part of the member, different geographical areas (i.e. Tvillingodden and the conodont fauna. Formation was defined in the western outcrop Above 108m, up to the last occurrence of area, while Sticky Keep Formationhlember was Wasutchites tardus, the polarity is normal (Vh), defined in the central areas). It should be noted that which corresponds closely with the normal the Russian researchers (e.g. PEelina 1983) polarity in the Sverdrup Basin sequences, covering presented correlations compatible with those made the same ammonoid zones. during the present study. Samples from the Vendomdalen Member have a The new Vikingh~gdaFormation type section is steeper mean inclination (entirely normal polarity) located in the same area as the earlier type section magnetization than the underlying units. It has not of the Sticky Keep FormatiodMember, but in a proved possible to test the age of this niagnetiza- well-exposed river section which permits both tion because of the low bedding dips. Combined palaeontological, sedimentological and magneto- with the reverse polarity in the Spathian identified stratigraphic control. The palaeontological control by Ogg & Steiner (1991) and Muttoni et al. (1995). (i.e. the presence of Arctoceras blomstrandi at these data suggest the Vendomdalen Member 98 m above base Triassic) clearly demonstrates the samples have been remagnetized. The cause of erroneous member boundary indicated by M@rk. the remagnetization is unclear - possibilities Knarud et al. (1982), and represents a clear include weathering and freeze-thaw action - but improvement in relation to the type section of may be causally connected with the following Buchan et al. (1965). features: Conodonts, palynomorphs and mineral grains I) The total dominance of an unidentified typical for the Kapp Starostin Formation are also magnetic sulphide as the carrier of the remanence recorded from the basal sandstone of the Deltada- in the Vendomdalen Member. len Member, indicating reworking at the boundary. 2) The exclusive collection of samples in the The Deltadalen Member is dated by the early Vendomdalen Member from the yellow weath- Griesbachian Otocerns boreale in the lower part of ering dolomite beds, of late diagenetic origin. the unit. The layers from 4.7-48.3 m are correlated Samples from other units were collected from by palynology to be of Griesbachian age. The age siltstone units, or early diagenetic calcite concre- is supported by magnetostratigraphy, which in- tions. dicates that sedimentation continued through the 3) The relatively high organic carbon content of Griesbachian into the Dienerian. Wignall et al. the Vendonidalen Member, which has probably ( 1997) have suggested that the presence of acted to modify the diagenetic processes respon- Tynzpariicysta stoschiuiza in the Vardebukta For- sible for the sulphides, in comparison to the mation as recorded by Mangerud & Konieczny underlying. less organic-rich units. ( 1991 1, could be associated with a Late Permian “fungal spike” (Visscher et al. 1996). According to The remagnetization is not a local phenomenon; the results presented by Mangerud & Konieczny recent work from the same unit at Milne (1993) and Mangerud (1994), a Permian acme 78 A. M@rk et al. zone for T. stoschianu has so far not been (Hochuli et al. 1989) predating the late Spathian recognized in Svalbard or on the Finnmark Plat- palynozone Svalis4 recorded in upper part of the form. At Vikinghogda the single specimen of T. Vendomdalen Member. stoschiana was discovered above the level of the The marked reduction in abundance of silt/ Otoceras boreale fauna. Therefore in Svalbard T. sandstones and the transition into dark grey stoschiana is only recorded well above the highest mudstones, which characterize the Vendomdalen records of Permian indicators like Vittutina spp. Member, occurjust above the sandstone bed with a and Vnellium spp. W. tardus Zone fauna. This transition correlates Biostratigraphical control in the Dienerian with transgressions in the latest Smithian in the deposits in Svalbard is poor with one observation Sverdrup Basin (Embry 1988, 1997) and in the of Vavilovites cf. sverdrupi (upper Dienerian) earliest Spathian in Siberia (Egorov & M~rkin from the Vardebukta Formation (Gazdzicki & press), and also correlates with a pronounced Trammer 1977) and one from Lusitaniadalen transgression in the Barents Sea (Van Veen et al. (KorEinskaja 1986). Palynology of the same level 1993). It should be noted that the change in reflects a change in the marine environment, abundance and type of organic material at the which continues into the Lusitaniadalen Member. Lusitaniadalen-Vendomdalen member boundary Throughout Svalbard no ammonite fauna has been indicates a change in sedimentary regime at this found in the lowest part of the Lusitaniadalen level. This change is accompanied by a minor Member or in the lowermost part of the Tvillin- reduction in sedimentation rate and a bloom in godden Formation. Classically an “undated am- marine plankton resulting in deposition of mixed monoid zone” is suggested at the base of the kerogen type IIRII. At the Svalis Dome, in the Smithian on most correlation diagrams (Mork. western Barents Sea, this transition is more Embry et al. 1989; Weitschat & Dagys 1989; prominent, resulting in the deposition of excellent Dagys & Weitschat 1993). The base of both the hydrocarbon source rock; a transition which is Lusitaniadalen Member and the Tvillingodden delayed until the Anisian Botneheia Formation in Formation have been interpreted as a major central Spitsbergen (MGrk & Bjory 1984). transgressive episode resulting in deposition of undated basal mudstones. This transgression has Acknowled~onents. - We wish to thank Reinhnrdt Veit for been regarded as earliest Smithian in age, partly ammonoid collecting, Clare Peters for co-work in the field and based on comparisons with other Arctic areas laboratory. and the technical staff at IKU/SINTEF Petroleum (Embry 1988; M~rk,Embry et al. 1989; Mork, Research, mainly Jan H. Johansen, for help with the illustra- tions. Discussions with Algirdas S. Dagys has clarified Egorov et al. 1994). The conodont N. svafharden- biostratigraphical problems. The project has been supported sis at 69m suggests an early Dienerian age. The by Saga Petroleum ASA and Norsk Hydro ASA. The manuscript magnetostratigraphic data indicate that the Delta- benefits from comments by Geoffrey Warrington and Aahton F. dalen-Lusitaniadalen member boundary is located Embry. within the mid-Dienerian, and that the basal parts of the Lusitaniadalen Member thus may be of Dienerian age. The palynological investigations allow recognition of the Assemblage N of References (Hochuli et al. 1989), with abundant ‘‘Fungal Balme. B. E. 1980: Palynology of Permian-Triassic boundary remains” below the first Arcroceras blumstrandi at beds at Kap Stosch, East Greenland. Meddefrlserom Gr@lczrid 98 m; and the present data show that Assemblage 20016), 37 pp. N starts already in the Dienerian. The well- Beauchamp. B.. Harrison, J. C. & Henderson, C. 1989: Upper developed overlying faunas document the E. Paleozoic stratigraphy and basin analysis of the Sverdrup romunderi and W. tardus zones (Fig. 13) which Basin. Canadian Arctic Archipelago. Part I: Time frame and tectonic evolution. 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Drnsnisporites pkiyfordi (Balme 1963) Playford Bull. Gd/f?.Sf. uf?il’.l//J.W/ti to, I 24-148. Wiman, C. 1916: Neue Stegocephalenfunde nus dem Pmidu- 1965 nomyaschiefer Spithergens. Bull. Ged. Inrt. Uiri~,.Upuh Densoisporites spp. 13(K). 209-227. Dictyotidium spp. Wiman. C. 1933: Uber Grippiii lonRirosfris.Nova Ac.ru Sot. SI i. Endosporites papillatus Jansonius 1962 Ups1rlu srr. 4, p. 9. Winsnes. T. S. 1981: Geological map of Svalhard 1 :XIOJJOO. Ephedripites sreevesii (Jansonius 1962) de Jersey \beet 2G. Edgeeya. Norvk Po/m+zsr.Skriftrr 154B. & Hamilton 1967 82 A. M@rk et a/. Filispliaericliirm .setci.seS.sitCiirte (Jansonius 1962) "Planktonic alga type A" Staph et al. 196.5 Poclosporites unzicirs Scheuring 1970 Foram linings Pol~citl~~ilatis~?oritesspp. "Fungal remain sp. B" Mangerud 1994 Pretricolpipollenites spp. "Fungal remains" Hochuli et al. 1989 Proprisporires pocockii Jansonius 1962 Cordonisporn fossulata (Balnie 1970) Van der Protodiplos.vpirius gracilis Scheuring 1970 Eem 1983 Protodil)lo.~~pitiu.sspp. Gmn~rlutisporitesspp. Protohciplplr~s~piiiiisniit~rocorpus (Schaarschmidt Grc~besporncoricenrric~~ Jansonius 1962 1963) Clarke 1965 I1lirzitc.s chitonoides Klaus 1964 Protohiiplo.~~~inir.spetfectiis ( Nauinova ex Kara- Ititi~~rrturopollrr?itrstiehiilosiis Balme I970 Murza 1952) Samoilovich 1953 Jerseyin.sporrr punctispinosu Kar. Kieser & Jain Prorolztiplo,.~~:\.l,irzussnrnoilovichii (Jansonius 1962) 1972 Hart 1964 Kliiir.sipollrtiite~sclziiirhergeri (PotoniC & Klaus Protohaplo.~~~,il,irl~sspp. 1954) Klaus 1963 Prerospertnellrr spp. Kme~r.reli.s~,oritr.supiciilurus Jansonius 1 962 Prrnctirtispor~itesfirngo.rrr.r Balme I963 KrrrcuscJlisporitrshoof&l(jkeri.si.s Visscher I 966 Reru.sorri1err.s hercyriicirs (Madler 1964) Schuur- K~iirii.selisl,or-itesspitlosirs Jansonius 1962 mann 1977 Kriri.iiseli.sl,orite.s spp. Retirsotriletes spp. Leeches cocoons Rrwunispom ,foivolatii de Jersey 1970 Leiospheres Stiipliiii.sl)[)rite.~ccinririirs (Balme 1957) Pocock Lirec~kisporirc~sjunior Klaus 1960 1962 Lirec~kisporitesvirkkiue PotoniC & Klaus 1959 Striurellu seebergensis Madler 1964 Lrrrititisporires rrc'iitus (Leschik 195.5) Scheuring Srriutoabieites halniei (Klaus 1964) Scheuring I970 1978 Liintrtisporires rioi~iuirlensi,~ (Leschik I 955) Striatoabieites rnidtistr'iatus (Balme & Hennelly Scheuring 1970 1955) Hart I964 Lirriafisporitrs pellirciiliis (Goubin 196.5) Balme Striurotibieites spp. 1970 Tusnitirzites Lirntcti.vporite.s spp. Triadisporu spp. Lunirrisporites tr(iir.si'er.siitidatrrsJansonius 1962 Tvmnpcinicystiz stoschicitiiz Balme 1980 Lr~ticlbla~is~~nmohsoleta Balme 1970 Unelliunr spp. LLlntlhltldi.sporl spp. Uvaesporitrs urgerituejiormis (Bolkhovitina 1953) Lyopodiiicidites spp. Schulz 1967 Mllclllutll.s~~or.itrsspp. Uim~sporitesiniperinlis (Jansonius 1962) Utting Micrliystridi~itiispp. 1994 Neomistrickiu spp. Verriicosisporites spp. Pechorosporitrs coronatiis Yaroshenko & Golu- Veryhachiiini subglobosirni Combaz. Peniguel & beva 1984 Vachey 1974 Prchorosporites tlisertiis Yaroshenko & Golubeva Venhtrclziirrn spp. 1989 Vesicusporii spp. Pechorosporites intern~edirisYaroshenko & Go- Vitreisporites pnllidirs (Reissinger 1938) Nilsson lubeva 1989 1958 Pilusporires spp. Vittutiriu spp.