Evaluar el nivel de cumplimiento de las metas presupuestarias en

In the latest Selandian (Thanetian) the first occurrence of Apectodinium sp. are recorded. In north France Apectodinium homomorphum has been recorded in the upper part of Thanetian III Bableu de Bracheux (Graus- Cavagnetto 1976a, 1976b, Chateuneuf & Graus-Cavagnetto 1978). In Belgium an assemblage containing sporadic Apectodinium spp. has been described by De Coninck et (1981) from the Sables d'Erquelinnes, and correlated with NP 9. This early Apectodinium event has also been recorded by Heilmann-Clausen (1985) from the Viborg 1 Borehole. This event seems to be missing from the upper part of the Thanetian section at H e m e Bay, but Heilmann-Clausen records the presence of Phthanoperidinium crenulatum in this section and suggests a correlation with the Apectodinium event. The Apectodinium spp. acme recorded by Hanson (1979a) is seen to follow this sporadic occurrence

(see Heilmann-Clausen, Viborg 1). Hanson (op.cit.) recorded this acme in the 01st and Fur Formations of Denmark. A similar acme has also been recorded in the Woolwich Beds (Downie et 1971, Costa & Downie 1976), the upper Landenian, Sables d'Ostende-ter-Streep in Belgium (De Coninck 1969, 1972, 1975b), the Spamacian of the Paris Basin (Graus-Cavagnetto 1976a, 1976b, Chateauneuf & Graus-Cavagnetto 1978), 01st Formation (Negative Series) in the Viborg 1 Borehole (Heilmann-Clausen 1985), and from most of the Forties Formation (IMit D) and Lower Sele Formation (Knox & Harland 1979, Knox et al, 1981, Powell 1988). In the Viborg 1 Borehole

the highest occurrence of Cerodinium speciosum glabrum is noted within this acme zone.

Following this Apectodinium spp. acme (basal Ypresian sensu Powell 1988) a change in dinocyst assemblage occurs, with abundant Glaphyrocysta ordinata and Deflandrea oebisfeldensis being recorded in the 01st Formation by

Hanson (1979a). Heilmann-Clausen et (1985) compared similar assemblages recorded in the Mo Clay (Fur Formation) to the 'ash series' in the North Sea and the ash-bearing sections of the London Clay at Harwich. Frequent G.ordinata were also recorded by lokim (1979) from the Balder Formation in the North Sea.

The first appearance of Wetzeliella spp. is seen in the Rosnaes Clay Formation (Fig. 29) with the successive appearance of Wetzeliella astra, W.meckelfeldensis and Eatonicysta ursulae taking place in the Knudshoved Member (basal Rosnaes Clay). At other Danish sections a condensed sequence may be developed at this interval (Heilmann-Clausen et 1985). Division A2 of the London Clay (King 1981), belongs to the Wetzeliella astra Zone and the lower part of the Wetzeliella meckelfeldensis Zone of Costa and Downie (1976) and Costa et (1978). Costa and Downie (1976) also report the W. meckelfeldensis Zone 3m above the base of the Argile d'Ypres in the Kallo Borehole, Belgium. In the Viborg 1 well Heilmann-Clausen (1985) notes the occurrence of sediments younger than the Wetzeliella meckelfeldensis Zone above the 01st Formation, i.e. Dracodinium similis Zone, D.

varielongitudum Zone and the Kisselovia coleothrypta Zone of Costa and Downie (1976), indicating a hiatus in this area. Within the W. astra and W. meckelfeldensis Zones, Vinken (1988) describes the abundance of

Spiniferites spp. and Achomosphaera alcicomu, and the restricted presence of Kisselovia crassiramosa (Fig 30).

Eatonacysta ursulae is noted by Vinken (1988) to occur in the upper part of the Knudshoved Member and in Bed Rl of the Rosnaes Clay (Subzone D 7a). This zone is dominated by Areoligera senonensis, with Thalassiphora

pelagica, Deflandrea phosphoratica and Hystrichokolpoma cinctum appearing within this zone.

The appearance of Dracodinium solidum is not used to define a palynozone by Vinken (1988), but Bujak et (unpubl. c.1986) describe this first

occurrence (Zone D 7a), which is associated with the first occurrence of D. similis and Homotryblium pallidum. Costa and Downie (1976) use D.similis as the defining event for the Dracodinium similis Zone, describing this zone from the London Clay, Argile d' Ypres (Belgium) and the Uhtereozan 2 (Meckelfeld, Germany). Equivalents of this zone have also been recorded from the Eocene of the North Sea by Knox and Harland (1978) and lokim (1979).

Palynozone D 7b of Vinken (1988) is defined by the first occurrence of Dracodinium varielongitudum. with D.condylos being restricted to this zone. Costa and Downie (1976) record the equivalent of this zone from the London Clay, Argile d' Ypres and (questionably) the lower part of the Uhtereozan 3. D. varielongitudum is also recorded in Bed R4 of the Rosnaes Clay (Heilmann-Clausen 1986). Bujak et al. (unpubl.) also recognise this

palynozone (D 7b), with Kiselovia edwardsii and Pthanoperidinium echinatum being seen for the first time. Costa and Downie (1979) record this event

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FIGURE 30. The dinoflagellate distribution in Eocene sediments of the Danish Subbasin. From Vinken (1988).

from the Rockall Plateau (DSDP, Sites 116, 117), Within this palynozone Vinken (op,cit,) reports the frequent occurrence of Areoligera senonensis, Thalassiphora pelagica and Eatonicysta ursulae.

The Kisselovia coleothrypta Zone of Costa and Downie (1976) is recognised by many authors including Williams and Downie (1966), Manum (1976), De Coninck (1977, 1978), Knox and Harland (1978), Costa and Downie (1979), Heilmann-Clausen (1985), Vinken (1988), Vinken (1988) notes the restriction of Ochetodinium romanum within this zone, with Samlandia chlamydophora and Dracodinium samlandicum being seen for the first time, Bujak et al,

(unpubl,) in recognising this zone (Zone D

8

The appearance of Areosphaeridium diktyoplokus is used by Vinken (1988) to denote Palynozone D 9, This zone has also been recorded in the middle part of Bed R

6

funiculatum, Wetzeliella aff, articulata, Homotryblium oceanicum, and the restriction to this zone of Wilsonidium tabulatum.

Bujak et (unpubl. c.1986) recognise within zone D 9 the last occurrence of E.ursulae. which coincides with the first occurrence of Areosphaeridium multicomutum (Zone D 10). Vinken (1988) does not use the highest

occurrence of E.ursulae to define a zone, this event being recorded within the Dracodinium pachydermum Zone. In sections from Jylland, Heilmann-

Clausen (1986) records the hipest occurrence of E.ursulae in bed L 4 (Fig. 29), which is associated with D.pachydermum. The dominant taxa in this interval include A .diktyoplokus. Systemotophora placacantha a M E.ursulae in the early parts of this interval (Vinken 1988). Taxa appearing in this palynozone include Areoligera undulata. Distatodinium paradoxum,

Cordosphaeridium cantharellum and Rhombodinium draco, extinctions include Adnatosphaeridium vittatum. D .pachydermum and Homotryfalium abbreviatum.

3.3 BIOSPRATTGRAPH Y OF SIÈCE BOUNDARIES

3.3.1 Maastrichtian/Danian Boundary

Although this boundary has not been encountered in the present study, it will be considered here for the sake of completeness.

Hanson (1976) discussed this boundary in onshore sections and boreholes in Denmark. The Maastrichtian was subdivided into three zones, the upper two zones correspond to the Palynodinium grallator Zone, which is subdivided into the Tanyospaeridium magdalium Subzone and the Thalassiphora pelagica Subzone. The T. magdalium Subzone contains the subzone species and

Palynodinium grallator ; the Thalassiphora pelagica Subzone contains the subzone species and Palynodinium grallator. The upper limit of the T.pelagica subzone marks the top of the Maastrichtian.

The Danian is marked by the Dania califomica Zone, which is subdivided into two subzones and three zonules. The Dania calif omica Zone is defined by the total stratigraphie range of D . calif o m i c a , which corresponds to all of the Danian. However, both Thomson and Heilmann-Clausen (1983) and

Heilmann-Clausen (1985) note the presence of a single specimen of

D. calif o m i c a in basal Selandian sediments. The Chiropteridium inomatum