PRANCE *"V \ 10. SITE 119. The Shipboard Scientific Party 1. Location: Cantabria Seamount, Bay of Biscay.

Transcription

1 0. SITE 9 The Shipboard Scientific Party Location: antabria Seamount, Bay of Biscay. Position: N, W; (satellite navigation). \ PNE *"V \ Depth of water: 4447 meters (corrected). \ ^W Total penetration: 7 meters. SITE BKGOUND ND OBJETIVES The origin of the Bay of Biscay (Golfe de Gascogne) has been discussed extensively in the past few years but there is no generally accepted mechanism by which it was produced. On the one hand it is proposed that the bay has been formed by the anticlockwise rotation of Spain and the consequent growth of oceanic crust by sea-floor spreading in the center. This view has been held in general by geophysicists and workers familiar with the oceanic crust. On the other hand, evidence from the neighboring continental geology, especially from the quitaine basin at the eastern end of Biscay, and from deep penetration reflection profiles across the Bay has been used to support a hypothesis of a sunken and oceanized continent underlying the thick sediments. These opposing views are discussed more fully in hapter 9, Site 8 and the evidence is summarized in Montadert et al. (97), and Debyser, Le Pichon and Montadert (97). The Bay of Biscay is extensively covered with thick sediments which make it difficult to sample the deeper layers. There are however four seamounts which rise above the abyssal plain. In the eastern Bay, "3270" Seamount (4.5 W) and Gascony Seamount (5.5 W) have not been studied in great detail. ecent profiles across Gascony Seamount suggest that it is underlain by downwarped continental rocks of Mesozoic age and older (Montadert et al.,. S. Laughton, National Institute of Oceanography, United Kingdom; W.. Berggren, Woods Hole Oceanographic Institution, Woods Hole, Massachusetts; ichard Benson, ugustana ollege, ock Island, Illinois; T.. Davies, Scripps Institution of Oceanography, La Jolla, alifornia; Ulrich Franz, Technische Hochschule, Munchen, W. Germany; Lillian Musich, Scripps Institution of Oceanography, La Jolla, alifornia; Katharina Perch-Nielsen, University Institute for Historical Geology and Paleontology, openhagen, Denmark; lan uffman, Bedford Institute, Dartmouth, Nova Scotia (Present address: Seascope onsultants, Box , PurcelTs ove, Nova Scotia); J. E. Van Hinte, Imperial Oil Enterprises, Ltd., algary, lberta;. B. Whitmarsh, National Institute of Oceanography, United Kingdom. 97). Both seamounts lie east of the region in which there is good seismic, gravity and magnetic control to support evidence for an oceanic crust. t the western end of Biscay, Biscay Seamount (0 W) lies outside the region which would have been formed by the simple anticlockwise rotation of Spain, although it does lie parallel to the fan-shaped magnetic anomaly pattern of the bay. antabria Seamount (8 W), on the other hand, lies well within the Bay at about 80 kilometers from the base of the continental slope north of Spain (Figure ), on a prominent E-W negative magnetic anomaly (Matthews and Williams, 968, Le Borgne and Le Mouël, 970) and over typical oceanic crust (Bacon, Gray and Matthews, 969). It was first surveyed with 5-mile spaced lines by Discovery-M in 966 (Jones and Funnell, 968) and the western end with 3-mile spaced lines by harcot in the same year (Vanney, 967). Subsequent surveys have been made by Vema-TI and by the Institute Francais du Petrole (IFP) in 969. The bathymetric chart (Figure 2) is based on British and French soundings up to 969. Seismic reflection profiles by airgun from Discovery-l showed a prominent reflector () overlain by about 0.4 second of a relatively transparent layer, dipping southward beneath the abyssal plain (Jones and Funnell, 968). On the north steep scarp reflector outcropped. Similar records were obtained by Vema-2 also with an air gun. However two crossings were made by harcot-9 in 969 using the Flexotir system, giving about 2 seconds penetration using a lower frequency (about 20 Hz). One section (Figure 3) was across the strike of reflector. t this frequency, reflector and the overlying transparent sediments are not so clear. In the "transparent" zone there are distinct reflectors dipping southwards, which lie unconformably on reflector which dips more steeply. Beneath reflector, there is a series of parallel reflectors to 2 seconds dipping to 753

2 SHIPBOD SIENTIFI PTY NOTH SPNISH MGINL TOUGH SPNISH ONTINENTL SHELF 0 W Figure. Bathymetry of the S.W. Biscay showing position of available seismic reflection profiles. Depths in corrected fathoms (Matthews 939). ontour interval 00 fathoms. the south at approximately 5 degrees. Some tentative correlation can be made with the layers seen on the E-W approach track of harcot-9 (Figure 4), but no continuity exists between these and the abyssal plain formations further west. Indeed it is likely that whole of formation and the top of formations 2 and 3 (defined by Montadert et al, 97) pinch out here against antabria Seamount. processed Flexotir profile (O 07) was shot by IFP across the seamount further east, in which nearly 3 seconds penetration was obtained (Figure 5). Gently dipping stratification was seen in the center section to 2 seconds. Montadert et al (97) correlate the formation between 0.3 and 2.3 seconds below the bottom as belonging to formations 2 and 3 found under the abyssal plain, although no continuity can be seen (Figure 6). Since Hole 9 penetrates 0.8 second, on this interpretation the lower part of the hole sampled formation 2. On the north scarp, cores and a dredge haul were made on Discovery- to sample reflector where it outcrops. Jones and Funnell (968) describe ore DY 5946 and Dredge DY 5948 both of which contain reworked pebbles of Maestrichtian coccolith ooze (see report on reexamination of this material in later section). lthough these are quoted to have been derived from 2400 uncorrected fathoms (4526 corrected meters), that is near the top of the cliff, further investigation shows that this was the echosounder depth derived from the side echo of the cliff and that the corer below the ship probably sampled the base of the cliff (Figure 7). It is possible therefore that these samples do not in fact represent reflector but some layer below it. Further attempts have been made to verify the existence of retaceous outcrops on antabria by IFP (Montadert, personal communication) and Vema-2, but the oldest sediment found has been Paleocene (Figure 2). The principle objective, therefore, of drilling a hole on antabria Seamount was to sample reflector (believed at that time to be retaceous) and to drill further into the layered sequence below it to obtain data on the older strata in the Bay of Biscay, since this site was the only place in Biscay where such old strata came within reach of drilling. 754

3 8 00'W D\ 05 IFP -r H0T-9 // / 45 00'N 0 KM 55 Figure 2. Bathymetry of antabria Seamount after Montadert (personal communication) showing position of available seismic profiles, and core and dredge samples. Depths in uncorrected meters at 463 m/sec. ontour interval 50 meters.

4 SHIPBOD SIENTIFI PTY NW D SE *.»...ΛN, <J ) LU H LU I LU ZD ca EFLETO EFLETO 2 B 2&3,:-,' *.-. _....f π< -,'. irf j. iifc -..i* i.','. '.«\. i 'i! V s». ".r. i.ii'.h'>v V. '. V. i..'...'.. h<i SES i ' V. O *. '"". N. L Λ it*. i' i t. " * '! * '. i.'..i ' '"'< iiii...' '.Λ'I's» i.''»*i.i i< *i*'i,* *',,».' ^,'.', T I ", i h,',' t,,d r,.i ' 'i * ' ' I Λ! ' I "H I, I 'i > "j f > i' ' h. i t*' H S ' ' 'i. " Figure 3. SE-NW seismic reflection profile D (Flexotir) by harcot-9 across strike ofantabria Seamount. Interpretation of layering by Montadert et al. (97) and by Sibuet et al. (97). (ecord by courtesy of.n.e..o., France.) 756

5 SITE 9 2&3 SES Figure 4. ^-PV seismic reflection profile B (Flexotir) by harcot-9 across SW end of antabria Seamount. (ecord by courtesy of.n.e..o., France.) Even so it was realized that at least 500 to 000 meters of stratified sediments would lie below the depth which could be sampled. secondary objective was to deduce the age of tectonic movement which thrust up antabria, if indeed it was at one time part of the deep-sea bed and not a continental remnant. In summary the objectives were: (a) To sample Maestrichtian and older sediments indicated by the reflection profiles. (b) To date the tectonic uplift of antabria Seamount. SUVEY DT The approach to antabria Seamount was made from the northwest. With no adequate navigation system on board, this had to be made by dead reckoning from Site 8, some 50 miles away, with one poor sun position line half way along. traverse of the seamount at 6 knots to the southeast normal to the strike direction was compared with the bathymetric chart based on the Discovery-\\ 5

6 SHIPBOD SIENTIFI PTY o IT) c K 00 O 2 ~ H σ cu o s- α> II ΠIP""'! "iv^ Vi r'""^'.''.?^^^ i i <..:'!; ó''.' \;.\ : f/; : i f 'W >/üffiiφ t o eg s- 2 - > JS o. +-> c <D o O rö I T3 8 α> II SS s Si I liiliiils üm 9 I I SES. Figure 6. NW-SE seismic profile FE by Glomar hallenger (80-60 Hz). oo o> \ to, l «^_ ^ ( r r o i.>wm '.y:;,vy; i i'/,vv; 0 a < ON fi fo fe. SJ Si. 3 if o co survey (the IFP chart was not at this time available); and it showed that we had crossed the most shallow area, and enabled an approximate position of the track to be determined. However, just as we started to cross the north cliff, the hydrophone eel became very noisy and had to be changed. It was necessary to replace it, by which time the seismic section was spoiled. The track was therefore reversed and a second profile made to the northwest, this time at 4 knots to give reduced noise and a more extended section. On this profile (Figure 6), the dipping reflectors which had been seen on the harcot-9 record were clearly seen, and a site for drilling was chosen at a depth of 4447 meters (corrected). The traverse was completed onto the abyssal plain, the track reversed again, and the seismic gear was recovered after we had once more reached the crest of the seamount. The beacon was finally dropped when the echo-sounder recorded a depth of 4447 meters (corrected). On completion of drilling, a profile across the beacon was made at 5.5 knots, from a point 2 miles to the northeast of the beacon in a direction 230 degrees thought to be approximately along the strike of the ridge of antabria Seamount, and for miles until well onto the abyssal plain. lthough navigation at the time was by celestial observation and dead reckoning, satellite fixes were recorded but not computed on board. track plot using the satellite 758

7 SITE 9 3KM ENE of Site r4500 <D Q SES Figure 7. Interpretation of bathymetric profile of antabria Seamount using the ellipse method (see text) and the principal reflecting horizons of profile EF. 759

8 SHIPBOD SIENTIFI PTY fixes computed subsequently required a current of 0.6 knots from the northeast in order to make the track consistent with the topography. The, relative position of the profiles of Glomar hallenger l and harcot-9 shown to be about one mile apart in Figure 2, is therefore open to some error. Furthermore, the beacon position lies west of both profiles shown in Figures 3 and 6. The hole positions have been shown in these figures at the equivalent water depth. Profile EF (Figure 7) has been corrected for beam angle by the ellipse method, which profoundly modifies the shape of the north cliff. Because the sound transmitted to the sea bed is not a narrow vertical pencil, echoes can be received from targets ahead, astern, or abeam of the ship. When crossing a linear feature at right angles, a geometrical construction can be used to translate the record into a profile which largely eliminates this effect. n ellipse is constructed which defines all points ahead and astern that lie at the range indicated by the echo time. By placing the apex of the ellipse on the recorded reflection at successive points, and tracing the ellipse onto the record, the true profile is formed by the envelope of the ellipses. It can be seen that all the echoes on the northern scarp are reflected from near the crest of the seamount. mean slope of 7 degrees has been calculated from the edge of the abyssal plain to the first reflecting point. However the echosounder record indicates some intermediate flatter areas and, hence, there must also be some steeper slopes. The seismic reflection record of the profile EF (Figure 6) showed a number of reflectors dipping to the southeast. Below the position of the site projected northeast onto this profile, the first major reflector is at 0.40 second below the sea bed. lthough it is not continuously strong, it can be traced (Figure 7) to the north scarp where it would outcrop at approximately 0.45 second above the abyssal plain (that is, 4536 corrected meters). This reflector correlates with reflector of Jones and Funnell (968) which is shown on their isopach map to lie at approximately the same depth along strike of the ridge. With this map, therefore, it can be correlated with the reflector shown on the harcot record at approximately 0.4 second at an equivalent position. However, the profile along the strike, (Figure 8) obtained after leaving the site, showed that reflector was very much more complex. series of hyperbolae to the northeast of the hole indicate that the region between 0.3 and 0.5 second is very distorted or fractured and that horizons although sometimes strong cannot be followed very far. There is some evidence that reflector is at about 0.45 second below Site 9. To the southwest of the hole, these hyperbolae are not seen, but this may be due to lack of energy. ssuming a velocity of.7 km/sec, reflector could correlate approximately with either the unconformity at 365 meters or with the harder layers drilled and cored at 420 meters and below. The next major reflector (2) on the Glomar hallenger profile EF was at 0.69 second dipping more steeply than reflector. This does not correlate with the strong reflector which shows at 0.32 second above the plain on the north slope and which is probably an exposed shelf. onsiderable energy is reflected in the 0.3 second below this shelf, perhaps because the transmitted sound enters the bottom at a favorable angle. The 0.69-second reflector (reflector 2) below the site more likely correlates with the shelf 0.8- second reflector above the plain (at depth 4745 corrected meters). On the harcot record (Figure 3), the equivalent reflector appears to be at 0.85 second and can be traced continuously to the base of the scarp. In the strike section, reflector 2 is more continuous under the site than reflector, and can be followed for 20 kilometers to the southwest. In Hole 9, hard siliceous limestones and hard clay beds were encountered at 592 meters and were drilled and cored for 6 meters below. The sudden reduction in drilling rate from 5 to 4 m/hr indicates the change of lithology which could correlate with reflector 2 giving a mean velocity from sea bed to reflector 2 of.7 km/sec. These hard formations are partially silicified limestones, silt and mudstones of Upper Paleocene age and turbidite facies. Below reflector 2, parallel dipping reflectors can be seen on the Glomar hallenger records (especially the 40 to 80 Hz record) down to.3 seconds below site. On the harcot record, they extend to about.9 seconds below sea bed. However on the Glomar hallenger record after drilling, the reflectors at.3 second below site converge with reflector until a confused series of reflectors appears at the southwestern end of antabria. The geophysical data indicates, therefore, that antabria Seamount cannot be considered to be a simple tilted block of stratified sediments. Both along strike and across it, there are zones of multiple hyperbolae indicating severe tectonism or diapiric intrusion. Strata can be correlated only over limited ranges and cannot be followed into the abyssal plain area. DILLING OPETIONS The beacon was dropped at 2225 hours on ugust 2nd in a water depth of 4447 meters (corrected). The bottom hole assembly of a Smith 3-cone tungsten carbide insert bit, 0 drill collars and 3 bumper-subs weighed 40,000 pounds. Bottom was felt at 0825 hours ugust 3rd, and a core was recovered from 0 to 9 meters. Thereafter cores were taken at 50-meter intervals until 250 meters. ecovery of these cores was not good, being less than 50 per cent. n attempt to increase recovery by coring extremely slowly with little weight, failed to improve this. Drilling became somewhat firmer at 200 meters. During the day on ugust 3rd, the beacon began to malfunction and transmitted on low power. second beacon was dropped and there was no loss of position. Below 250 meters, continuous cores were taken in order to find and identify the unconformity suggested from the seismic profiling in the region of 250 to 350 meters. It was expected that the Paleocene lay close to the unconformity and that the Maestrichtian lay close beneath this. However this was not to be. n unconformity was indeed found at 356 meters but between Lower Oligocene and lower Middle Eocene. Paleocene was not reached until 400 meters at about which level some harder patches were encountered. ores were cut with 20 to 30 Klb on the bit and with 5 to 0 s.p.m. on one pump. ontinuous cores were cut down to 433 meters, but still we were in the Upper Paleocene. Hard layers were found between 370 and 440 meters which could explain the 760

9 SITE 9 SES Figure 8. Interpretation of seismic reflection GH by Glomar hallenger after leaving Site 9. reflectors thought to be Maestrichtian on the basis of correlation up-dip to the Discovery-\\ core sample, but these turned out to be due to the upper part of a thick Paleocene turbidite sequence containing silty limestones. The rate of cutting core decreased from 60 m/hr to about 30 m/hr. Several times when the rate of cutting dropped very low it thought to be due to balling up of clay on the bit, but on slicing the cores, hard silicified layers were found. The increased rate of sedimentation in the Upper Paleocene led us to open out the coring interval. Drilling proceeded with the core barrel in, but with high circulation, and to cut the core the circulation was reduced. The theory was that no core would be recovered with high circulation, but in fact the harder layers were recovered and the softer layers were washed away. ores 28 to 32 (433 to 594 meters) were cut this way. There is doubt about where, in the drilling plus coring interval, the core actually came from; and, the convention was used here that it all came from the coring interval. Penetration was about 5 to 20 m/hr. ore 33 (594 to 600 meters) cut extremely slowly, and high circulation was needed to make progress at 6 m/hr. The core barrel was withdrawn because we wanted to know the nature of the hard layer. It was gray muddy silicified limestone, of lower Upper Paleocene age. 76

10 SHIPBOD SIENTIFI PTY Hole ore * 36* 37* 38 39* 40* TBLE ores ut at Site 9 ored Interval (m. subbottom) *More than 9 meters cored, see text. ore ecovered (m) In order to progress, perhaps faster, the center bit was run down instead of the core barrel for the interval 600 to 622 meters. irculation pressure had to be reduced to prevent the drill string "bouncing" too hard on the bottom. The center bit was recovered in anticipation of taking a core, but when the core barrel was down, faster progress was made for a while before it became hard again. fter ore 34 was recovered at 235 hours, ugust 6th, the drill string was lifted off the bottom of the hole and drilling stopped. Winds up to 35 knots made it necessary to transfer power from the drill platform to run the main propulsion. The winds moderated at 0245 hours, ugust 7th and drilling was resumed. From the top of ore 35 (630 meters) to the bottom of the hole at ore 40 (7 meters) drilling became progressively slower varying from 4 to 2 m/hr using moderate circulation. The coring interval varied from 2 to 8 meters, and core recovery of hard limestone and siltstone averaged about 6 meters, representing the harder layers encountered in the coring interval. ores were obtained about every 6 hours. The last one, ore 40 (699 to 7 meters) was brought to the surface at 755 hours, ugust 8th, 5.5 days after the first core. During the last phase of cutting ore 40, the circulation became blocked. Gray clay was recovered from the bit when it was brought to the surface. lay from the jets in the bit was sampled separately as it must represent the lower strata in the hole. The bit was not worn too badly, and it had been drilling in the hard strata for over 2 days. total of 92 meters of core was recovered out of 368 meters cut in 40 cores (52.2 per cent). The weather at the site varied from flat calm and light northerly winds to 35 to 40 knot winds from the southwest with heavy rain squalls. Swell was small. LITHOLOGY ore descriptions for each of the 40 cores recovered from Site 9 are given in an appendix to this chapter. The sedimentary section cored on antabria Seamount can be divided into two main parts: calcareous silty clays (ores to 8) above and red clays and turbidites (ores 9 to 40) below. The hole terminated at 7 meters below the seabed in the turbidite sequence. These two lithologic sections can be separated on the basis of visual examination. Paleontological studies (q.v.) show that the upper sequence is Oligocene to ecent in age, whereas, the lower is Paleocene to Middle Eocene, clearly indicating a hiatus in deposition. Further subdivision of the section is difficult, but each of the two parts can be broadly subdivided as shown on the following page. However, the transition from one lithology to another is gradual and compositionally these units are not discretely defined (Figure 9). ppendix shows the results of an examination of the smear slides. s with the other sites, preliminary analyses of grain size and carbonate content were made on samples taken from the cores in order to better define the lithologies. The results are shown in Figures 9 and 0 and ppendices B and 762

11 SITE 9 Depth (m) - 0- ore No. Lithology %a Olive gray silty clay 03 α> 03 α> Soft gray nannofossil Light olive nannofossil gray clay Olive gray, greenish gray and dark greenish gray hard nannofossil clay. Pale yellow and pale olive nannofossil clays with blue-white bands in ores 4=7 Brown and dark brown mottled clays. 03 to o c: α> σ> s~ Ter LU] 03 S- o on oo O 4- oo 3 O D (J OO Gray calcareous clays & silts (turbidites) 500 O Some red clay bands Figure 9. Summary of the section sampled at Site 9, showing variations in carbonate content and in occurrence of prominent sedimentary components. Depth Below Seabed (m). The coarse fraction recovered in the course of grain size analysis was examined and the results are displayed in Figure. Oligocene ecent silty clays Paleocene Eocene sediments Olive gray silty clays (ores and 2) Gray, greenish-gray and yellow nannofossil clays (ores 3 to 8) ed brown and gray clays (ores 9 to 24) Turbidites The Paleocene and Eocene Sediments (ed lays and Turbidites) These sediments are all recrystallized, indurated calcareous sediments. The turbidites beds form a series of gray marls and soft calcarenites, alternating with red clays and soft calcarenites, and with intervening layers of pelagic sediment (Figure 2). In many places the turbidites show lamination, convolute bedding and other primary sedimentary structures (load casts, etc.), see Plate. Some samples suggest grading, but this is not so clearly developed as in the turbidites sampled at Site 8. ecrystallized foraminifera and large lumps of soft, chalky limestone are the dominant coarse sedimentary components, suggesting that, like the Miocene turbidites sampled in ores 7 and 8 763

12 SHIPBOD SIENTIFI PTY LY EOENE PELGI SEDS. OES l-2 o 3-8 D9-24 -( OLIGOENE TO PLIOENE PELGI SEDIMENTS SND Figure 0. Texture of samples from Site 9. SILT at Site 8, these turbidites are derived from loosely consolidated calcareous shelf deposits. possible source for these sediments is the northern part of the quitaine Basin which shoaled and changed shape considerably at the end of the Mesozoic (Bonnard et al, 958). The major earth movements in the quitaine are Eocene. In addition to the carbonate, some quartz grains, volcanic glass, pyrite and nannofossils were seen. The finer part of the turbidites consists in some places of a gray marl and, in other parts of the section, especially nearer the bottom, of a brick red clay. The gray marl presumably represents normal, fine-grained calcareous pelagic sediment derived either from the shelf or from the deeper parts of the Bay of Biscay traversed by the turbidity currents. The red clays, on the other hand, are probably derived from areas with metamorphosed ("baked") sediment or from areas of lateritic weathering. Since the red clays in this part of the section are confined to the finer parts of discrete turbidite beds, it can be assumed that alteration of the clays took place before their deposition as a part of the turbidite sequence. If, as seems more plausible, the clays are in fact the product of mild metamorphism or "baking," this could have taken place either in the marine environment (Boström and Peterson, 969) or on land, since Post-Mesozoic basalt intrusions are known on the neighboring continents. It might be suggested that the alternation of red and gray clays suggests deposition near the "compensation depth" and that this depth varied from time to time. However, it should be emphasized that the red and gray clays form the upper parts of turbidites and that comparable variations are not seen in the intervening pelagic sediments. This sediment is a smooth indurated nannofossil marl, pale green in the lower part of the section, but darker green toward the top. The pelagic sediments have been extensively burrowed (alectorurid type), the burrows being flattened along the bedding planes by subsequent compaction (Plate 2). The beds appear to dip at 0 to 20 degrees, and slickensides were seen in ore 764

13 SITE 9 i>o BUNDNT OMMON E SMPLE NUMBE QUTZ & FELDSP DK MI LIGHT MI OTHE DETITL MH PYITE GLUONITE DETITLBONTE PLNKTONI FOMS BENTHONI FOMS SILIEOUS FOSSILS FISH TEETH OTHE FOSSILS < )) i( i> i i i» Figure. omposition of the coarse fraction of samples from Site 9. TUBIDITE PELGI TUBIDITE PELGI TUBIDITE PELGI TUBIDITE PELGI TUBIDITE PELGI '6). Q LU H < cπ D Q LU H >- <c H D > >- D o H H ZD Q Figure 2. Schematic section of turbidite sequence, showing relationship between variously colored lithologies. 37, further suggesting deformation (Plate 3). The carbonate content of both pelagic sediments and turbidites is highly variable and ranges from 4 to 84 per cent. For about 50 meters above the turbidite sequence there are red, white, brown and gray-brown clays. These are essentially the same in composition as the fine sediments in the turbidite sequence, being mostly composed of detrital carbonate and clay minerals, but they have a conspicuous contribution of hematite and limonite indicating oxidizing conditions (relative to the dark green pelagic sediment in the upper part of the turbidite sequence). few foraminifera and fish debris are the only significant coarse constituents. Since the boundaries of the different colored clays are _l Q 765

14 SHIPBOD SIENTIFI PTY irregular and apparently unrelated to bedding (compare with red clays in turbidite sequence below), it seems likely that the red coloration and associated mineralogy of these clays could be associated with nearby volcanism, rather than being a function of depositional conditions (Boström and Peterson, 969). These clays are of similar age and lithology to the altered red clays found in ores 5 through 9 (685 to 750 meters subbottom) from Site 8. Nannofossil lays bove the brown and red clays, at 355 meters subbottom, is clearly a hiatus in deposition for the character of the sediments changes abruptly and the paleontology indicates a break in the stratigraphy. The sediments above the break, from 75 to 355 meters below the seabed are nannofossil clays, hard but not lithified or recrystallized. Furthermore, the characteristic structures and textures resulting from turbidity current deposition disappear. This suggests that it was during the hiatus in sedimentation that antabria Seamount was affected by earthmovements and changed from a topographic low receiving abundant turbidite sediments to a topographic high receiving only pelagic sediment. It might be pointed out that this point in time coincides with the major earth movements in the Pyrenees and the quitaine (Bonnard et al., 958). Nannofossils remain the dominant constituent of the sediments, along with pyrite and clay minerals. Volcanic glass is a noticeable constituent at many levels, especially in ores 8, 9 and 5. Siliceous fossils (adiolaria and sponge spicules) are noticeable in ores 5 through 3 and foraminifera down to ore 5, below which they become rare. Fish debris is common throughout, probably a result of the slow rate of accumulation of these sediments. These sediments, even in the coarse fraction, still contain noticeable amounts of quartz, feldspar and mica flakes and have a certain detrital aspect with rare grains of garnet, tourmaline, etc. Thus, it is more appropriate to call them nannofossil clays rather than oozes (compare Sites 6 and 7). Texturally they are classed as silty clays and can be distinguished from the pelagic sediments found in the Paleocene and Eocene (see Figure 0). The carbonate content of these sediments is variable but seems to generally decrease upwards in the succession, indicating an increased contribution of mineral material through time. The terrigenous (mineral) material must be brought from the shelf off Brittany and the quitaine by either suspended transport in the water mass of the Bay of Biscay, or from the dilute tops of turbidity currents which must occasionally overtop the seamount. The increase in the amount of terrigeneous material with time suggests the latter may be the case. These sediments are burrowed more or less extensively (chondrites type) throughout. Silty lays The top 75 meters of sediment cored (ores and 2) consist of olive gray silty clays. These are the same as the nannofossil clays below, but the terrigenous component is markedly greater. The higher rate of sedimentation both here and at Site 8 during the late Pliocene and Pleistocene indicates that turbidity currents have been more active, associated presumably with the erosion of the continental shelf during the period of lowered sea level during glaciation. Ice-rafting may also have increased the sedimentation rate. The presence of reworked retaceous and Oligocene nannoplankton in the Pleistocene silty clays indicates that the tops of these turbidity currents traveling on the abyssal plain contribute to the sediment on top of the seamount. PHYSIL POPETIES The physical properties of the sediments at this site are well defined because of the large number of cores recovered. Disturbed or watery cores were rarely encountered (mostly ores 9-, 9-2 and Sections 9-0-6, 9--6, 9-9-4, 9-9-6, , 9-2-6), but many of the harder cores became fragmented by transverse breaks during drilling and this is noticeable from ore 28 onwards. The above two effects gave rise to aberrant low GPE densities, and these have been allowed for in drawing trend lines on the density, impedance and porosity plots. In the first 300 meters density increases on average from.5 to.85 gm/cc. Velo.city measurements and the penetrometer similarly indicate increasing firmness of the sediment over this interval. In detail, however, density appears to increase more rapidly between 0 and 50 meters and between 260 and 300 meters with a less rapidly changing region between 50 and 260 meters, but the reason for this is not apparent. The gamma activity measured within the interval zero to 300 meters is extremely variable but averages about 300 counts. lthough the onset of glaciation must lie above 50 meters, it is not apparent from the gamma activity when this occurred. Even though ores and 2 have higher counts than ore 3, other cores immediately below 3 also have higher activity than this core. In the lower part of the interval gamma activity increases to 2500 counts in Section then abruptly drops to around 500 counts. The higher counts seem to be associated with a greenish-gray clay. The drop in activity is associated with an abrupt lightening of sediment color. The fairly constant lower gamma activity below 270 meters seems to be due to a higher carbonate content since 7 spot values from ores 9 to 3 gave contents between 46 and 70 per cent, while 3 samples from ores 6 to 8 gave values between 8 and 40 per cent. The interval 300 to 356 meters is occupied by Oligocene sediments. Density decreases on average in this interval from.9 to.8 gm/cc. Velocity is fairly constant but also decreases in the interval 348 to 356 meters from.7 to.6 km/sec. The reason for these two trends is not clear but they are not associated with a decrease in grain size, or with a softening of the sediment according to the penetrometer which shows a continuing increase in firmness around this depth. The Oligocene clays show extraordinary high gamma activity with several sharp peaks, the highest of which reaches 4650 counts. Strangely, the three biggest peaks in ores 4 and 5, and three lesser peaks in ore 7, are 766

15 SITE 9 associated not with dark sediment but with pale blue or pale olive bands in a pale yellow nannofossil clay. The only carbonate measurements in these cores (66 per cent at , and 70 per cent at ) were associated with counts of 000 and 500. The first measurement rules out the possibility that the peaks are due to a lack of carbonate, and enrichment in uranium, thorium or potassium is suspected. t 356 meters, there is an abrupt increase in gamma counts between ores 8 and 9 from 450 to 700 counts. t the same depth, density and velocity also increase. These changes are due to crossing an unconformity separating the Oligocene nannofossil clays from brown and dark brown mottled Eocene clays. Sediment firmness does not increase noticeably across the boundary. Below the unconformity density fluctuates between.8 and 2.0 gm/cc and shows no systematic trend. Between 400 and 450 meters velocity starts to increase and does so steadily to the bottom of the hole. The average gamma activity seems to decrease below the unconformity from about 200 to about 600 counts, although there are several peaks well above this average level. The greatest of these peaks (3600 counts) occurs at 405 meters in association with a brown clay band. The sedimentation rate at this time was about 0.25 cm/000 yrs. The nearest carbonate sample ( ) contained 2 per cent carbonate yet gave a count of only 900. Therefore it seems highly likely that the peak at 405 meters is due to uranium and thorium enrichment. There are five distinct peaks below the biggest one. The uppermost four ( , , , ) are all associated with dark gray clay lying immediately over a much lighter colored clay with a sharp boundary in between. These horizons are clearly the bases of turbidity current layers and presumably contain concentrations of radioactive detrital minerals. The deepest peak is at and occurs in a red brown clay. The cores at this site show the correlation between natural gamma activity and darkness of the sediment very well. Numerous examples can be found throughout the hole, especially in the Paleocene, possibly indicating reducing conditions at the sea floor. Nevertheless the -ray results from ores 9, 8, 9 and 29 suggest that darker sediments contain more mica, and this may be partly responsible for the correlation since biotite often contains inclusions of radioactive accessory minerals as well as potassium which is also present in muscovite. The concurrence of light blue sediments with high gamma activity in the Oligocene is unique to this site for Leg 2. Depth of eflectors Two reflectors were picked from the reflection profile crossing the site. eflector at 0.45 second is discontinuous, and adjacent profiles show it to have an irregular surface. The impedance plot suggests that the unconformity at 356 meters gives rise to this reflection since the impedance changes just above it. The second reflector was observed at 0.69 second and is relatively continuous laterally. It appears very likely that this reflection comes from the same depth where the drilling rate suddenly decreased. t this depth (595 meters) velocities of up to 2.7 km/sec were encountered for the first time. These reflector data are summarized in Figure 3. General PLEONTOLOGY ND BIOSTTIGPHY The hole bottomed at 7 meters in indurated limestones of Early to Late Paleocene age (approximately the Danian-Thanetian boundary), short of an anticipated rendezvous with the retaceous-tertiary boundary. In contrast to the site in the abyssal plain in the Bay of Biscay (Site 8), the sedimentologic sequence appears to be reversed here, that is, the upper 400 meters are essentially of pelagic origin, whereas an approximately 300-meter thick Upper Paleocene sequence of turbidites occurs below. The stratigraphic sequence is probably complete from the Pleistocene to the Lower Oligocene. n unconformity at about 360 meters separates Lower Oligocene from Middle Eocene sediments. Below the Pleistocene the cores exhibit evidence of selective solution as indicated by the fact that the planktonic foraminiferal fauna is strongly reduced in most of the Oligocene, Miocene and Pliocene samples and virtually absent in the Paleocene and Eocene samples. This would suggest that this site has been at or below calcium carbonate compensation depths throughout most of the enozoic. summary of the foraminiferal biostratigraphy at Site 9 is presented in Figure 4. DEPTH M Figure 3. Two-way travel times below the sea bed of observed reflections plotted against the downhole depths of horizons believed to have given rise to these reflections. The mean velocity to the deepest reflection associated with a definite depth is given close to the line representing this velocity. 767

16 SHIPBOD SIENTIFI PTY T in my EPOH SEIES OES (9) FOMINIFEL PLNKTONI BIOSTTIGPHY BENTHONI (2) 3 (5) PLEISTO. PLIOENE LU O o L M G. inflata G. tvunoatulinoides G. ovassula + G. punaticulata Globoquadrinids Pyvgo muvvhyna Lectio, halophova Mel. pompilioides Epist. exigua Plan, aviminensis E OLIGOENE Globigevinita dissimilis + unioava \ & ib. tvinóherasensis ib. gvimsdalei ib. havanensis nom. pompilioides nom. semioribvata EOENE,- small aoavininids Nuttallides truempyi lab. dissonata 30 o LU 3 Turbidites with few Foraminifera T.D. 7 egular 9 m core drilling w. center bit followed by coring; precise core-recovery interval not determinable Figure 4. Foraminiferal biostratigraphy at Site 9. Discussion Pleistocene Foraminifera The Pleistocene is represented by ores (0 to 9 meters) and 2 (50 to 59 meters). Temperate-water planktonic faunas in these cores are dominated by Globorotalia inflata, G. crassaformis, Globigerina bulloides and Orbulina universa. Globigerina pachyderma occurs in both cores in moderate numbers. The presence of Globorotalia truncatulinoides in both cores supports the Pleistocene age determination. Such deep-water benthonic foraminifera as Pyrgo murrhynα, Melonis pompilioides, Epistominellα exiguα, Eponides tener, Lαticαrininα hαlophorα characterize these cores. Pliocene The Pliocene-Pleistocene boundary is drawn at about 75 meters on the basis of upward extrapolation of sedimentation rates (using an age estimate of 3 million years for ore 3 at 00 to 09 meters). ore 3 contains a rich planktonic foraminiferal fauna which is subtly different from the Pleistocene faunas in ores and 2. The association of Globorotalia puncticulata, Globorotalia crassula and early forms of G. crassaformis (similar to G. crassaformis ronda of Blow) is similar to that observed at other sites in the course of Leg 2. In pre-upper Pliocene sediments the occurrence of typical Globigerinoides obliqua also suggests a Pliocene age and this is supported by the assignment of ore 3 to the Discoaster surculus Zone (see below). The benthonic microfauna of ores to 3 and, indeed, of the succeeding cores below (4 and 5) consist primarily of 768

17 SITE 9 deep-water fauna belonging to the genera Gyroidina, Pullenia, Melonis, ibicidoides, Pyrgo, Eponides, Planulina, Laticarinina, Eggerella, Ehrenbergia, and Stilostomella; various nodosariids and lagenids are also present. Many of these forms appear to have been recorded from piston cores from the Gulf of Biscay by French paleontologists and it is not surprising to see these forms extending back into the Miocene and Pliocene in this area. Miocene The Miocene-Pliocene boundary is drawn at approximately 40 meters (on the basis of extrapolation of sedimentation rates). The Miocene is represented by ores 4 (50 to 59 meters) through 0 (276 to 285 meters). The Oligocene-Miocene boundary has been tentatively drawn at about 280 meters (that is within ore 0) again on the basis of extrapolated average sedimentation rates. ore 4 is of Late Miocene age based on age determination of calcareous nannoplankton. The planktonic foraminifer al fauna contains Globigerina praebulloides, G. atlantica and G. nepenthes, which indicates merely that ore 4 can be placed within the limits of Zones N4 through N6. The planktonic foraminifera in ore 5 (98 to 207 meters) are mostly dissolved. few specimens of Globoquadrina dehiscens and a globorotaliid similar to G. acostaensis were found in the ore atcher sample. ore 5 is of Middle Miocene age according to the calcareous nannoplankton flora. significant change in fauna can be seen between ores 5 (98 to 207 meters) and 6 (240 to 249 meters). ore 6 is of Early Miocene age, at least in its lower part where planktonic foraminiferal fauna containing Globigerinita dissimilis, G. unicava, Globoquadrina praedehiscens, G. dehiscens, and Globorotalia siakensis, among other forms, occurs. The benthonic foraminiferal fauna is also distinctly different from that occurring above and has its closest affinities with Oligocene-Miocene foraminiferal faunas found below. mong the forms identified from ore 6 are nomalinoides pompilioides,. semicribrata, ibicidoides trincherasensis, and. grimsdalei. ore 6 is the highest level at which these various benthonic foraminifera occur at Site 9. The planktonic foraminiferal association indicates an age not younger than Zone N6 Globigerinita dissimilis becomes extinct at the top of Zone N6. The bottom of ore 6 has been assigned to the Helicopontosphaera ampliaperta Zone (see report below). ccording to the Leg 2 shipboard correlation chart the H. ampliaperta Zone correlates with Zones N7 and N8. The present data suggest that the base of the H. ampliaperta Zone may overlap the upper part of Zone N6. ontinuous coring was initiated with ore 6 (240 to 249 meters) and extended over almost 200 meters to ore 27 (428 to 433 meters). Planktonic foraminifera are rare in the Lower Miocene sediments which consist primarily of gray calcareous clay and silts with abundant radiolarians (see report below). When they occur, the forms present are referable to Globigerinita (G. dissimilis and G. unicava) and Globoquadrina (G. praedehiscens and G. dehiscens). Oligocene It is not possible to draw an Oligocene-Miocene boundary on the basis of planktonic or benthonic foraminifera at Site 9. On the basis of extrapolated sedimentation rates and Oligocene-Miocene boundary is drawn at about 280 meters, that is, within ore 0. This agrees with the age assignment of ores 8 through to the Discoaster druggi- Triquetrorhabdulus carinatus Zones, and of ores 2 to 4 to the Sphenolithus ciperoensis Zone (see below). The Oligocene is represented by ores (285 to 294 meters) to the upper part of ore 9 (356 to 365 meters). The unconformity between Lower Oligocene and Middle Eocene is put at about 360 meters (within ore 9). Globigerinita dissimilis and G. unicava are the dominant forms in the generally impoverished planktonic assemblage in the Oligocene. n important biostratigraphic marker, Globorotalia opima, occurs in ore 4 (3 to 320 meters). This is the youngest occurrence of G. opima at this site and its occurrence together with chiloguembelinids suggests that ore 4 is equivalent to the lower part of Zone P2. ores 6 (329 to 338 meters) through 9 (356 to 365 meters) contains poor planktonic faunas in general. n exception was noted within ore 7, where although the diversity is low, Globorotalia opima nana occurs quite commonly. Solution is believed to be responsible for the relative paucity of planktonic foraminifera in these as well as other cores at Site 9. The benthonic foraminiferal fauna in the Eocene, Oligocene and Lower Miocene at Site 9 exhibits a continuity of development, which attests to the stability of the deep sea environment, despite possible tectonic movements between Middle Eocene and Early Oligocene time. These faunas exhibit a marked affinity with Lower and Mid- enozoic faunas described from the aribbean region. In particular, the Eocene and Oligocene faunas show a strong affinity with those described by Beckmann (953) from the Middle Eocene-Oligocene sections on Barbados. The similar association of planktonic and benthonic foraminifera, radiolarians and calcareous nannofossils here in what must have been abyssal depths during the Eocene-Oligocene and Early Miocene strongly supports the idea that the Barbados section also was deposited at similar depths. The Eocene faunas (ores 9 through 24) are characterized by the following forms: Nuttallides truempyi, labamina dissonata, Bulimina grata, ibicidoides havanensis, ibicidoides trinitatensis, Oridorsalis ecuadorensis and various stilostomellids, nodosarellids and ellipsodimorphinids. In particular the stilostomellids appear to dominate the benthonic fauna quantitatively, although Nuttallides truempyi is the single dominant species. This group of forms is supplemented, and in some cases replaced, by additional forms in the Oligocene such as: ibicidoides grimsdalei, ibicidoides martinezensis, Gyroidina octocamerata, Gyroidina perampla, nomalina alazanensis, and Vulvulina jarvisi. Various species of the agglutinated genera Gaudryina, Karreriella and Dorothia occur commonly in the Eocene, Oligocene and Lower Miocene assemblages. They appear to have been described originally from the Trinidad area and their presence here in the Bay of Biscay testifies to their widespread distribution. Eocene ores 9 (356 to 365 meters) to 24 (40 to 40 meters) are tentatively assigned to the Middle and Early Eocene, the 769

18 SHIPBOD SIENTIFI PTY benthonic and planktonic foraminiferal faunas becoming gradually poorer as one proceeds downwards and it is not possible to draw a clear distinction between the Early and Middle Eocene. Paleocene The Paleocene-Eocene boundary is tentatively drawn at about 40 meters (between ores 24 and 25). thick (about 275 meters) Paleocene turbidite sequence is developed from about 40 meters (ore 25) to about 675 meters (ore 37). With the exception of ore 25 (40 to 49 meters) there are practically no foraminifera within this entire stratigraphic interval, with the exception of minute, usually indeterminable forms in the fine fraction of the residues. ore 25 (40 to 49 meters) contains Globigerina triangularis, G. velascoensis, Globorotalia aequa, Globorotalia pasionensis, and carinina coalingensis and is assigned to Zone P5 (Late Paleocene). The lower part of the Upper Paleocene was found in ore 38 (674 to 686 meters) based on the presence of Globorotalia pseudobulloides, G. varianta, G. angulata, G. conicotruncata, G. ehrenbergi, and Globigerina triloculinoides. This faunal association indicates a level within the upper part of Zone P3. ores 39 (689 to 699 meters) and 40 (699 to 7 meters) may have penetrated somewhat older sediments. The association of Globigerina spiralis and Globorotalia angulata in ore 40 suggests that the oldest sediments cored at this site are of earliest late Paleocene age and referable to the top of Zone P2 or base of Zone P3. alcareous Nannoplankton fairly complete sedimentary sequence from Paleocene to Pleistocene was cored at this site, with only the Late Eocene missing. The sediments consist of pelagic clays (sometimes with glacial influence, sometimes with a touch of turbidite) and turbidites. The site on antabria Seamount was chosen, among other reasons, with reference to previous descriptions (Jones and Funnell, 968) of Late retaceous sediments recovered from the antabria Seamount. s the Late retaceous was not reached where it was expected, if it outcropped on the seamount (see Figure 7), the sediments described by Jones and Funnell (968) were re-examined together with other cores taken subsequently by Vema-27 and IFP. Examination of these samples leads to the conclusion that there is no evidence that Late retaceous sediments have been recovered on antabria Seamount. n account of these further studies follows this section. The rather high percentage of retaceous coccoliths in some of the Leg 2 samples is noteworthy. In all cases, younger coccoliths were found together with the retaceous forms. t Site 8, which lies on the abyssal plain 75 kilometers from Site 9, the highest core, taken 00 meters below the sea floor, contains up to 90 percent retaceous coccoliths besides the Pleistocene assemblage. Such a sample, taken by dredging or a surface core, might well be mistaken as retaceous with Pleistocene contamination. Pleistocene ores and 2 contain rather poor Pleistocene coccolith assemblages. They represent the Gephyrocapsa oceanica and the occolithus jaramillensis Zones. In both cores, a minor amount of reworked Late retaceous and Oligocene coccoliths was found. The assemblages are, in fact, as poor as those from the Northern tlantic Pleistocene. Scapholithus fossilis and yclococcolithus macintyrei are present in ore 2 but missing in ore. occolithus pelagicus is again present in different varieties. Pliocene No attempt was made to sample the Pliocene-Pleistocene boundary or the onset of glaciation at this site. The Pliocene-Pleistocene boundary was placed arbitrarily halfway between ores 2 and 3. s there also occurs a change in Lithology between these two cores it is reasonable to put the onset of the influence of glaciation in the Bay of Biscay there, too. In ore 3, there is no evidence of glacial rafting and it can be assigned to the Discoaster surculus Zone. Thus, the glacial influence must have started later than this, which means at the same time or maybe only a little later than at the other sites where the onset of glaciation was dated. This was expected. With the data available from this leg, no more precise time can be given than between 3 and about.5 million years ago. The Pliocene is represented only by ore 3, that contains an assemblage including Discoaster surculus but lacking eticulofenestra pseudoumbilica. eworked coccoliths include Prediscosphaera cretacea (retaceous) and yclococcolithus neogammation (Oligocene-Miocene). Miocene ores 4 to? contain Miocene assemblages; from ore 6 on, coring was continuous. In ore 4, a rich discoaster flora is present, but it is composed solely of long-ranging species. It contains very well-preserved discoasters similar to D. subsurculus, but with the branches of the arms almost touching each other. Similar discoasters were found in Hole, together with Discoaster quinqueramus. s in the latter hole, Triquetrorhabdulus rugosus is also present. ore 4 is therefore regarded as representing Late Miocene. In ore 5, the discoasters are not as well preserved as in ore 4. They include D. deflandrei, D. aulakos and D. exilis, suggesting assignment of the core to the D. exilis Zone of the Middle Miocene. In ore 6, the Sphenoliihus heteromorphus and the Helicopontosphaera ampliaperta Zones are present. ore 7 represents the Sphenolithus belemnos Zone, while in ore 8 Triquetrorhabdulus carinatus is present. The Miocene-Oligocene boundary lies somewhere between ore 9 and ore 3 and cannot be determined with calcareous nannofossils at this site. Generally, the Miocene assemblages are somewhat richer in discoasters than those found in the northern tlantic. n exception to this is the Middle and Late Miocene of Site, where similar abundance and greater diversity occurred. Oligocene While the very top of the Oligocene lies somewhere in the interval ores 9 to 3, in the lower part of ore 4, we find the Sphenolithus distentus Zone, that also is represented by ore 5. The normal succession continues downward with the Sphenolithus predistentus Zone in ores 6 and 7, the Helicopontosphaera reticulata Zone in ores 7 770

19 SITE 9 and the upper part of 8 and the Ericsonia obruta Zone in the lower part of ore 8. In most samples sphenoliths are quite common, but never abundant. The short-ranging forms as S. ciperoensis, S. distentus and S. predistentus are far less common than the small, undescribed sphenoliths and S. moriformis that has a very long range. Generally the assemblages are monotonous and the preservation of the coccoliths is only fair throughout the continuously cored Oligocene. eworked coccoliths include Eocene and Late retaceous forms in small amounts. Eocene Eocene is represented by ores 9 to 24. pparently, the uppermost Eocene is missing. Throughout the Eocene, calcareous nannoplankton is represented mainly by discoasters, the coccoliths having been dissolved. mong the coccoliths that sometimes are present are different species of hiasmolithus, Ericsonia cava, E. lternans and eticulofenestra sp. The uppermost third of ore 9 is believed to belong to the Discoaster tani nodifer Zone; while in the lower part, this uncommon species is missing. The Nannotetrina fulgens Zone is represented by part of ore 9 to ore 22. In this core 22 Nannotetrina is missing in a sample with a very poor assemblage in Section 2 and in a somewhat richer, gray-brown sediment of the core catcher. In creamcolored sediments of the core catcher, however, Nannotetrina cristata is present again. The top of ore 23 has a discoaster assemblage typical for the Discoaster lodoensis Zone. Thus the Discoaster sublodoensis Zone is either missing or represented in the interval between ores 22 and 23 that was not recovered. In ore 23, the Marthasterites tribrachiatus Zone is also represented. ore 24 is barren with the exception of the core catcher that contains a discoaster assemblage typical for the Discoaster binodosus Zone of the Early Eocene. The Marthasterites contortus Zone was not found but could be present in the interval between ores 24 and 25 that was not recovered. Paleocene The change in Lithology between ores 24 and 25 also defines a change in the content in calcareous nannofossils. occoliths are preserved together with the discoasters in the turbidite samples, while discoasters are relatively more abundant in the pelagic upper part of the turbidites (see Figure 5). The flora found in the Paleocene of this site, especially in the upper part, is very rich and in some samples very well preserved. It is similar in content to the Paleocene described by Hay and Mohler (967) and Martini (96) from Pont Labau in Southwestern France and by Bramlette and Sullivan (96) from the Lodo Formation of alifornia. The stratigraphic assignment of ores 25 to 40 is shown in Figure 5, together with the occurrence of selected species. Especially diverse in this section are the fasciculiths. These small bodies, that in the light microscope look very simply constructed, showed a greater diversity than previously known. In addition to the three known species, nine new ones are described from this site (Perch-Nielsen, 97). Work in progress with the scanning electron microscope also revealed a variety of ruciplacolithus tenuis with prominent extensions to one side of each quarter of the central cross (See hapter 5). In the genus hiasmolithus, we find a small to H over a small central opening in the lower part of the section (ores 37, 38) together with forms with a large, wide H over a more extended central area. t least from ore 28 upward, a net may be present and preserved between the bars of the H. Beside Ellipsolithus macellus and E. distichus, another coccolith, perhaps belonging to Ellipsolithus, was found (see hapter 5). In this section, it seems possible to find the early evolution of the Sphenolithaceae and the Fasciculithaceae, as well as, the Discoasteracea, Heliolithacea and the Tertiary part of the Zygodiscaceae and Pontosphaeraceae. The other two big Tertiary families, the occolithaceae and the Prinsciaceae have their development earlier than the age of the oldest sediments recovered. From ore 28 downward, Braarudosphaera, represented by the species B. bigelowi, B. discula and B. imbricata, became more abundant and may constitute up to 20 per cent of the coccolith assemblage in a few samples in ore 39. This could indicate restricted conditions of the sea in the Bay of Biscay at this time. The amount of reworked and well preserved coccoliths varies throughout the hole, but, except for the cores of Eocene age, reworked coccoliths are always present, even in pelagic oozes. This reflects the fact that turbidity current derived deposits have been laid down in the abyssal plain in the Paleocene and again at least since the Oligocene (see discussion of sedimentation rates). Even if no coarse material has been deposited on the seamount itself, older coccoliths were mixed with the water and settled down with the coccoliths of the time. s for the Paleocene turbidities, the coarser fraction is also present and contains a nannoflora of mixed Paleocene and Late retaceous. e-examination of Discovery-7 Material and ores by Vema-27 and Institute Français du Pétrole Introduction In 966, Discovery-W attempted to sample reflector on antabria Seamount. The following account summarizes the findings of Jones and Funnell (968). The core taken at Station Dy5947 proved to consist of a Pleistocene calcareous ooze without signs of contamination by Tertiary or retaceous microfossils. Bottom photographs nearby had shown many light-colored angular or subangular pebbles and occasional boulders lying on a sediment-covered slope, without clear evidence of rock outcrops. The core taken at Station Dy5946 consists in the lower part of a conglomerate of calcareous ooze and clay of different shades of white, gray, and red set in a clayey matrix. The calcareous nannoplankton yielded by the white, off-white and light gray pebbles consisted of abundant Upper retaceous genera including rkhangelskiella, Microrhabdulus, Micula, Zygrhablithus, Braarudosphaera and Zygolithus. Dark pebbles consisted of unfossiliferous clay. In the matrix, lower and/or middle Tertiary discoasters and coccoliths were found together with retaceous forms. The few foraminifera found are small and represent the Upper retaceous, lower/middle Tertiary and the Pleistocene and are mixed together. 77

20 SHIPBOD SIENTIFI PTY Figure 5. Nannofossil distribution chart. The uppermost 80 centimeters of this core consist of almost entirely noncalcareous and unfossiliferous clays. The top two centimeters howevef contain calcareous nannoplankton of middle to late Tertiary age. Small foraminifera of middle Tertiary and Pleistocene age were also found. The dredge Station D5948 yielded approximately 50 discrete lumps of clay and slightly indurated ooze. Here too, Upper retaceous, most probably Maestrichtian calcareous nannoplankton was found, while foraminifera of Late retaceous age were absent or rare and Pleistocene foraminifera were abundant. 772

21 SITE 9 In conclusion, Jones and Funnell (968) suggested, that fine parts of Maestrichtian turbidite sediments had been sampled at a near-outcrop and that reflector is Late retaceous, probably Maestrichtian in age. s the Late retaceous on Site 9 was not reached where it was to be expected if it did outcrop on the seamount (see Figure 7), the sediments described by Jones and Funnell (968) were re-examined. lso examined were samples from cores collected by Vema-2 and by the Institut Francais du Pétrole in 969 in an attempt to sample further Late retaceous sediments from antabria Seamount. The samples from Vema-2 were kindly provided by the Lamont-Doherty Geological Observatory. ONLUSIONS The results of the re-examination of the samples collected by Discovery-W, Vema-2 and IFP are listed in Table 2. No attempt was made to determine the age of the samples down to the zone, because the purpose of the re-examination was mainly to check on the evidence for outcropping Late retaceous sediments. In the samples studied, no such evidence could be found. The samples with up to 90 percent Late retaceous coccoliths all also contain Paleocene or younger coccoliths. On Site 9, no such high percentages of reworked Late retaceous coccoliths were found in the Paleocene turbidites. However on Site 8, 00 below the bottom, the Pleistocene turbidites also contain about 90 percent Late retaceous coccoliths. Jones and Funnell (968) have already suggested that their Late retaceous sediments are fine parts of turbidites. This opinion is supported by the results of drilling at Site 9, however the age of the turbidites is younger than Late retaceous; most probably the oldest pebbles belong to the Early Paleocene (ruciplacolithus tenuis Zone), while other pebbles show Late Paleocene assemblages including Fasciculithus. (Neogene coccoliths, where present, are rare and probably the result of contamination when the conglomerate was formed.) The dark clay-pebbles might represent the pelagic part of the Paleocene turbidites that were deposited below the calcium carbonate compensation depth, since in the Paleocene turbidites of Site 9, it was observed that the dark pelagic part had very few coccoliths compared to the predominantly coccolith composition of the fine material at the top of the lower part. However, burrowing has in some instances obscured this pattern. alcite (or dolomite) rhombohedrons are present both in the Discovery, Vema and IFP samples, and the Paleocene turbidites of Site 9. They seem here to be restricted to Paleocene sediments and unfossiliferous sediments where no age assignment was possible. lso the samples provided by Vema-2 and IFP show no evidence for Late retaceous sediments outcropping or within reach of surface cores. enozoic adiolaria Well-preserved, common to abundant radiolarians are present only in the Lower Miocene of Hole 9. s a result of downhole caving these assemblages also occur, often abundantly but mainly in core catcher samples, from as low in Hole 9 as ore 25 (Upper Paleocene). Occasional contaminant specimens are found from within the cores themselves. Zeolitized, silicified and corroded radiolarians are present in most of the remaining cores (Oligocene-Paleocene), but only the silicified and/or corroded Paleocene specimens are biostratigraphically diagnostic. Several well-preserved middle Eocene species occur as contaminants in 9-36-, but no source for these was found higher in the Eocene section of the hole. Miocene The first downhole occurrence of radiolarians is in ore 5 which is dated tentatively as middle Miocene on the presence of digitately branched Oroscena spines. lthough assemblages from 9-6, Sections and 2 (78 to 79 centimeters) include most of the species present in the alocycletta virginis Zone, the very rare occurrence of alocycletta costata (iedel) suggests the inclusion of this interval within the. costata Zone of early Miocene age (hapter 6, Table 2). The interval through 9-7- is placed questionably within the. virginis Zone because of the occurrence in 9-7- of a specimen of. costata, but because of the known downhole contamination in Hole 9 little significance should be placed on the presence of this species in a core catcher sample. ores 9-8 through 9--, 69 to 70 centimeters contain well-developed assemblages typical of the alocycletta virginis Zone of early Miocene age. Oligocene-Eocene The interval from 9--2, 75 to 76 centimeters through 9-2- is dated as Oligocene on the absence of typical Lower Miocene species and the presence of yclampterium (?) sp. cf.. (?) milowi iedel and Sanfilippo. The remaining Oligocene and all Eocene cores (3 through 8 and 9 through 24, respectively) contain poorly to moderately preserved, undiagnostic radiolarians. lterations of the siliceous skeletons ranges from minor corrosion through silicification through complete replacement by zeolite. In this interval radiolarians are generally rare or absent but are common to abundant in some samples from ores 6, 9 and 25. Several fish teeth are present in and 3 (Eocene). Many resemble those illustrated by Helms and iedel (97), particularly their D-types. Paleocene The highest occurrence of Paleocene radiolarians in Hole 9 is in ore 26-2, 8 to 82 centimeters. The silicified and/or corroded assemblages, which may comprise perhaps 25 to 30 species in some samples, are rare to common through ore 30, absent in ores 3 through 34, rare to common in ores 35 and 36, and absent in ores 37 through 40. Zeolitized radiolarians are more abundant than the silicified or corroded forms. Diagnostic Paleocene species present include Lithocampium sp. iedel and Sanfilippo (in press), which is the dominant species, Phormocyrtis striata Brandt, and Bekoma bidarfensis iedel and Sanfilippo (in press, Plate 7, Figure 7). In addition, one specimen of (T)mphipyndax stocki (ampbell and lark) was observed from the Lower Paleocene of Hole 9, ore 36,. (See hapter 6, Plate 2, Figures 0, ). 773

22 SHIPBOD SIENTIFI PTY TBLE 2 esults of the re-examination of smearslides of samples collected by Discovery, Vema-2 and IFP Late retaceous occoliths Tertiary occoliths emarks ge of the Sediment 46, (2ore ollector Samples LB 2.B 3.B 4.B 5.B 6.B 7.B 8.B 9.B 0.B lay alcite rhombohedrons Eiffellithus rkhangelskiellaceae ribrosphaera Others ruciplacolithus tenuis hiasmolithus danicus Ericsonia cava Fasciculithus Discoasters Miocene? No coccoliths No coccoliths No coccoliths No coccoliths Very few coccoliths No coccoliths No coccoliths No coccoliths Few retaceous coccoliths in Paleocene P = Paleocene P N = Neogene N T = Tertiary T.B 90% retaceous coccoliths 0% Paleocene P o Disc 2.B 3.B Few retaceous coccoliths in Paleocene Few retaceous coccoliths in Paleocene P P 4.B Very few coccoliths N 5.B Few retaceous coccoliths in Paleocene P 6.B Few retaceous coccoliths in Paleocene P 7.B Few retaceous coccoliths in Paleocene P 8.B Few retaceous coccoliths in Paleocene P? T 9.B 90% retaceous coccoliths 0% Paleocene P 20.B 90% retaceous coccoliths 0% Paleocene P 7d Very few coccoliths - Tertiary T 8b Few coccoliths, D. multiradiatus P <o 5948, E>redj 9b 2 3b 28b Very few coccoliths - Tertiary Very few coccoliths - Tertiary retaceous & Paleocene retaceous & Paleocene P P T T >very. 35b 39b Tertiary Paleocene & few retaceous coccoliths P N? T y 4b Paleocene & few retaceous coccoliths P 43b 47d Paleocene & retaceous Paleocene & Neogene P P N 48 retaceous & Paleocene P 774

23 SITE 9 TBLE 2 - ontinued Late retaceous occoliths Tertiary occoliths emarks ge of the Sediments ollector Samples 73 lay alcite rhombohedrons Eiffellithus rkhangelskiellaceae ribrosphaera Others ruciplacolithus tenuis hiasmolithus danicus Ericsonia cava Fasciculithus Discoasters Paleocene & few retaceous coccoliths P = Paleocene N = Neogene P T = Tertiary 79/ Paleocene & few retaceous coccoliths P I.F.P. 79/2 79/3 Paleocene & few retaceous coccoliths Paleocene & few retaceous coccoliths P P 80/ Few coccoliths, Paleocene & few retaceous P 80/2 Few coccoliths, Paleocene & few retaceous Top Pleistocene & few retaceous N 5 cm Pleistocene & few retaceous N 40 cm Pliocene & few retaceous coccoliths N Vema-2, 30 Vema-2, 32 Vema-2, cm 0 cm 40 cm 80 cm 220 cm 240 cm 4 cm 4 cm 20 cm 32 cm 35 cm 70 cm 50 cm 249 cm 30 cm 70 cm 90 cm 20 cm 50 cm 80 cm 220 cm 240 cm 280 cm Pliocene retaceous, Paleocene, Eocene, Oligocene Few coccoliths, Paleocene & few retaceous Paleocene & few retaceous coccoliths Paleocene & few retaceous coccoliths Paleocene & few retaceous coccoliths Miocene-Pliocene Miocene Miocene Miocene No coccoliths Miocene Miocene Miocene Few coccoliths, Pleistocene No coccoliths No coccoliths Paleocene & few retaceous coccoliths Paleocene & few retaceous coccoliths Paleocene & few retaceous coccoliths Paleocene & few retaceous coccoliths Paleocene & few retaceous coccoliths Paleocene & 70% retaceous coccoliths N P P P P z z z z z z z N P P P P P P T 775

24 SHIPBOD SIENTIFI PTY Downhole ontamination mple evidence of downworking of sediments from above in Hole 9 during drilling and coring operations exists in the presence of Lower Miocene radiolarian assemblages representing the alocycletta virginis Zone in samples as old as Upper Paleocene. Downworking is suspected even within the. virginis Zone in core catcher samples from ores 8, 9 and 0. Very rare to abundant radiolarians from this zone occur in core catcher samples of ores through 6, 9, 2, 22, and 25. In fact, the best assemblage representing the. virginis Zone occurs as contamination in 9- (Eocene). Minor contamination occurs also within the cores themselves in the following samples: 3-3, 70-7 cm; 4-4, cm; 54, 7-73 cm; 6-3,0- cm; 20-3, 2-3 cm; 2-2, cm; and 26-2, 8-82 cm. The origin of this contamination may be from a rind immediately adjacent to the inner surface of the core liner. Middle Eocene ontaminants There is a rather mysterious contamination of Middle Eocene radiolarians from the Theocampe mongolfieri Zone (see iedel and Sanfilippo, 970) in one sample from the core catcher of ore 36. Some 25 to 30 species of wellpreserved adiolaria are represented by only one or two individuals each. No other samples from the core catcher have these contaminants. Examination of samples from the Eocene interval of Hole 9 (ores 9 through 24) revealed only a few very poorly preserved specimens in situ. The source of the Eocene contaminants apparently is not to be found in Hole 9. Perhaps some of the coring equipment which may have cored radiolarian-rich Middle Eocene sediments on a previous leg of the Deep Sea Drilling Project is to blame. Just a small amount of such sediment left in a core catcher would be enough to supply the observed contaminants. It should be noted that none of these wellpreserved species were found at any of the other Leg 2 sites drilled. ESTIMTED TES OF SEDIMENTTION It would appear that average rates of sediment accumulation at Site 9 were relatively high during the Paleocene and during the Late Pliocene and Pleistocene. The average rates during the Eocene, Oligocene, Miocene and Early Pliocene were relatively low. The differences in rate can probably be ascribed to the following causes: Paleocene turbidite deposition; Late Pliocene-Pleistocene larger terrigenous component owing to glaciation; Eocene-Early Pliocene pelagic deposition coupled with the modifying effects of calcium carbonate solution. ge determinations, upon which the estimated average rates of sedimentation have been calculated for Site 9 are as follows: ) 3 million years. ore 3 (00 to 09 meters); early Late Pliocene (D. surculus Zone); 2) 5 million years. ore 6 (240 to 249 meters; Early Miocene based on assignment to upper part of Zone N6; 3) 29 million years. ore 4 (3 to 320 meters; early Late Oligocene based on assignment to lower part of Zone P2; 4) 53 million years. ore 24 (40 to 40 meters), Paleocene-Eocene boundary based on approximated boundary between D. multiradiatus and D. binodosus Zones (calcareous nannofossils); 5) 59 million years. ore 38 (674 to 686 meters), early Late Paleocene based on assignment to upper part of Zone P3. It can be seen from Figure 6 that rates of sedimentation have varied considerably during the enozoic on the site of antabria Seamount. Paleocene turbidites yield expectedly high rates of sedimentation. These are followed by the lower rates normally associated with deep-sea pelagic sedimentation, but the effect of calcium carbonate solution has certainly played a major role in lowered sedimentation rates due to the removal of the planktonic foraminiferal elements. The fluctuating rates during the Late Oligocene, Miocene and Early Pliocene may reflect real conditions which existed in the seas at the time or they may reflect minor inaccuracies in the time scale used in our calculations. lternatively, they may indicate stratigraphic hiatuses, but no evidence of this is seen from the faunas which we have examined. hiatus does occur, however, at about 360 meters, and separates Lower Oligocene from Middle Eocene. The approximate time represented by this hiatus is about 8 million years and it is during this time that antabria Seamount was uplifted above the level of the abyssal plain. During the Late Pliocene and Pleistocene the rates increased to about 3.7 cm/000 yrs (uncorrected), reflecting the increased amount of terrigenous detritus in the form of glacially-rafted debris as well as the larger contribution of clay and silt from the increased turbidity current activity during lowered sea level. Higher productivity is also associated with Pliocene-Pleistocene glaciation. In Figure 6, dates derived from coccolith determinations (in millions of years) for Holes 8 and 9 are plotted against depth (in meters). Successive points for each hole are connected by a line. Only above 300 meters does there seem to be a systematic density gradient, and this gradient of gm/cc/m can be used for correcting sedimentation rates above 300 meters for the effects of natural consolidation. The 3. cm/000 yrs rate above 00 meters becomes 3.5 cm/000 yrs, and the average rate between 00 and 300 meters increases from 0.9 to.5 cm/000 yrs. DISUSSION Forty cores were taken at Site 9. total of 92.4 meters were recovered from the 368 meters cored. The hole bottomed at 7 meters in indurated limestones of early Late Paleocene age. relatively complex sequence of enozoic sediments appears to be present on antabria Seamount. n unconformity which separates Lower Oligocene and Middle Eocene strata was encountered at about 360 meters. This hiatus represents a time-interval of about 8 million years. The uplift and tilting of antabria Seamount probably occurred during this interval. The sequence of sedimentation appears to be reversed at Site 9 compared to Site 8. The upper 400 meters of sediment on antabria Seamount are primarily of pelagic origin. Below 400 meters, a thick (approximately 300 meters) sequence of turbidites of Late Paleocene age was encountered. 776

25 SITE 9 ESTIM. VE. SED. TE cm/ooo yrs. LEOUS NNNOPLNKTON T.D. Ill Figure 6. Estimated average sedimentation rate at Site 9. Identification of reflecting horizons Two principle reflecting horizons have been noted on the seismic profiles of antabria Seamount, although many others exist above and below them. They have been discussed in detail in the section on survey data. eflector marks the top of a sequence of beds apparently dipping to the southeast overlain unconformably by beds dipping less steeply in this direction (Figure 3). long strike, the reflector is not continuous and may have been eroded subsequent to the uplift of antabria Seamount or perhaps fractured by tectonic activity, although the continuity of deeper reflectors opposes this explanation. Under Site 9, it is at 0.45 second, equivalent to 380 meters at.7 km/sec, although this depth could be in error by ±30 meters. t 356 meters, there is an unconformity of 9 million years between Middle Eocene turbidites and red clays, and Oligocene nannofossil clays. Drilling met hard layers from 367 meters onwards and these changes are reflected in the impedance plots from the physical properties. eflector is associated therefore with the top of the sediment sequence which accumulated prior to uplift of antabria Seamount in the Middle to Late Eocene. Some erosion may have removed any Late Eocene sediments. lternatively, Late Eocene sediments initially may have accumulated after the uplift in a depression on the southeastern flank of the seamount, and the unconformity under Site 8 kept clear of BSLT sediments by bottom currents until this depression filled. This would explain the onlap of the upper sediments. Sibuet et al. (97) distinguish three formations (, B and ) above the unconformity. Formation, of 200 meters thickness, is thought to lie on a minor discordance of Upper Miocene age, for which we find no evidence. Formations B and are interpreted as pelagic sediments lying on top of the unconformity but slumped to the southeast following further tectonic disturbances. Sibuet et al correlate formations, B and with the flatbedded turbidite sequences of the surrounding abyssal plain which at Site 8 were sampled as far down as Lower Miocene, but which may extend into the Oligocene. lthough this correlation may be valid from the point of view of age, the facies above reflector in Hole 9 is markedly different from that of the top 700 meters of Hole 8. eflector 2 is widespread and continuous below central antabria Seamount and outcrops at a depth of 4745 meters on the northwestern scarp (30 meters above the abyssal plain). t Site 9, it was at 0.69 second and has been correlated with the sudden reduction of drilling rate at 590 meters when the hole penetrated the indurated clays, limestones and calcarenites. The increase in acoustic impedance at this depth would explain the reflector. The age of this horizon is Late Paleocene (58 million years). 777

26 SHIPBOD SIENTIFI PTY Sibuet et al. (97) divide the sediments below reflector into Upper D and Lower D formations. eflector 2 lies in the lower part of Upper D formation. The boundary between Upper D and Lower D outcrops on the northwestern scarp at the level of the abyssal plain, and is dated by Sibuet et al. as the top of the Maestrichtian on the basis of Jones and Funnell (968). However, a re-examination of this material, described above, concludes that the samples of Jones and Funnell, are Paleocene and that the Maestrichtian coccoliths have been transported from elsewhere. n extrapolation of a mean sedimentation rate of 4.6 cm/000 yrs (measured for the Late Paleocene) throughout the Paleocene would place the Maestrichtian-Paleocene boundary at 955 meters. t a mean velocity below reflector 2 of 2.5 km/sec, the boundary should be at 0.98 second. This corresponds with the boundary between Upper and Lower D formations which would barely outcrop at the foot of the northeastern scarp. Sediment horizons can be seen on the harcot-9 record down to.6 seconds below the sea bed at Site 9. ssuming a velocity of 2.5 km/sec, this would be at a depth of 700 meters. t a sedimentation rate of 5 cm/000 yrs for the Upper retaceous, the age of the deepest horizon would be 80 million years. The Search for Maestrichtian Sediments n objective of Hole 9 was to penetrate reflector, believed before we drilled, to be Maestrichtian and outcropping on the northeastern scarp (Jones and Funnell, 968). The failure to reach Maestrichtian at 7 meters, well below reflector, prompted a re-examination of the Discovery-\\ data which Jones and Funnell studied. Two points emerged. () lthough the recorded echo sounder depth at the time of coring Station 5946 was 4256 meters (corrected), thereby placing the sample near the top of the northeastern scarp, this was probably, in fact, a side echo. n analysis of the profile (Figure 7) shows the probable depth under Station 5946 to have been about 4800 meters (corrected), that is, near the base of the scarp. The correlation by Jones and Funnell with their reflector, is therefore probably erroneous. (2) re-examination of samples from Stations 5946 and 5948 by K. Perch-Nielsen in direct comparison with Hole 9 cores led her to the conclusion that the oldest samples were Paleocene although containing up to 90 per cent reworked retaceous coccoliths (see report above). Jones and Funnell recognized that the retaceous material was reworked but suggested that it has been locally derived. The presence of retaceous contamination throughout the stratigraphy of Hole 9, suggests that the contamination comes from further afield. The erosion of retaceous outcrops (Stride et al. 969) on the continental margins around the Bay of Biscay by turbidity currents could provide this material. Turbidity currents could be considerably slowed down by meeting the north cliff of antabria Seamount and some of the suspended sediment load could be deposited, the finer material reaching the top. Tectonic Uplift of antabria Seamount The sediments below the Middle Eocene/Oligocene unconformity have been recognized as turbidites and pelagic red clays deposited below the carbonate compensation depth, whereas those above are pelagic nannofossil clays. The sediments indicate a tectonic uplift of antabria at this time as discussed above. The unconformity probably represents an erosional surface after the uplift of antabria Seamount during the Middle or Late Eocene. The underlying sediments show evidence of this tectonic disturbance. omparison of Sedimentation onditions at Sites 8 and 9 Graphs of sediment accumulation against time are shown in Figure 6, and a comparison of the two resulting curves leads to the following conclusions and speculations. In Paleocene time a thick turbidite sequence accumulated at Site 9, whereas at Site 8 volcanic rock was exposed or being formed (?). The location of 9 apparently was deeper than 8, the lower site receiving turbidite sediments. During latest Paleocene and Early Eocene time pelagic sediments were deposited at both sites, whereas a part of the Middle and Late Eocene were times of erosion and subsequent nondeposition. t Site 8 the period of nondeposition continued until Middle Miocene time. This is probably due to the topography of the basement, Site 8 being on the side of a basement high and, as can be seen on the seismic profile, (Figure 5) sediments were deposited on the lower parts of the basement south of Sites 8 and 9. Extrapolating mean sedimentation rates of Miocene turbidites found at Site 8 (4 cm/000 yrs) to the maximum thickness of the layered sediments in the north Spanish Marginal Trough (2.5 seconds equivalent to 3000 meters at 2.4 km/sec), one can conclude that they are of retaceous age. The apparent continuity of layering suggests a continuity of sedimentation there since retaceous. Paleocene turbidites at antabria Seamount show that this was subject to the same sedimentation regime, whereas the Eocene/ Paleocene red clays of Site 8 suggest that this was a local ridge during this period. Tectonic uplift of Sites 8 and 9 probably occurred simultaneously in the Middle to Late Eocene. fter this, Site 9 was practically free of turbidites until the Middle Miocene; and, it may be assumed that the seamount stood well above the sea floor in Oligocene and Early Miocene time, receiving pelagic sediments only. From Middle Miocene until the present day, the influence of the upper part of the turbidity currents might be the reason for the progressively higher sedimentation rate. This could indicate that the seamount did not rise further relative to its surroundings, its relief becoming less and less pronounced because the sediments were being deposited around it at a high rate. The Evolution of the Bay of Biscay The Bay of Biscay has received considerable attention in the last few years, both on the continental margins, especially in the quitaine Basin in the southeastern corner, and in the deep ocean. Much new data is currently being published (cf. I.F.P.;.N.E..O. Symposium sur 'histoire structural du Golfe de Gascogne/Debyser et al, 97, and it is inappropriate here to do more than make some observations based on Holes 8 and 9. Le Pichon et al. (970; in press) have developed theories of the relative plate movements of Spain and France, and the formation of 778

27 SITE 9 the Pyrenees. Sibuet and Le Pichon (97) discuss the north Spanish Marginal Trough. comparison of the tectonic movements of Sites 8 and 9 during the Late Eocene with those reported in the quitaine basin (Bonnard et al, 958) suggests that they occurred at the same time (Figure 7). Following each phase of earth movements the Biscay abyssal plain received floods of turbidites (getting progressively finer upwards) of carbonate debris which had accumulated up-slope probably off the quitaine, prior to the earth movements. The formation of red clays, accumulated at both 8 and 9 prior to the interruption of sedimentation, might be associated with volcanism nearby, preceding the tectonic disturbance, as suggested by Boström and Peterson (969). The data of 8 and 9 provide some key dates for the development of the Bay of Biscay, but a complete understanding of its history must await the synthesis of these with the theories both of the Biscay region and of the north tlantic as a whole (for example: Pitman and Talwani, in press, Williams and McKenzie, 97, and Laughton, 97. EFEENES Bacon, M., Gray, F. and Matthews, D. H., 969. rustal structure studies in the Bay of Biscay. Earth and Planet Sci. Letters, 6, 377. Beckmann, J. P., 953. Die Foraminiferen der Oceanic Formation (Eocaen-Oligocaen) von Barbados, Kl. ntillen. Eel Geol. Helv. 46 (2), 30, 30 pis. Bonnard, E., Debourle,., Hlauschek, H., Michel, P., Perebaskine, V., Schoeffler, J., Seronie-Vivien,. and Vigneaux, M., 958. The quitanian Basin, Southwest France. In Habitat of Oil Weeks, L. G. (Ed.). Tulsa (m. ssoc. Petrol. Geol.) 09. Boström, K. and Peterson, M. N.., 969. The origin of aluminum-poor ferromanganoan sediments in areas of high heat flow on the East Pacific ise. Marine Geol 7, 427. Bramlette, M. N. and Sullivan, F.., 96. occolithophorids and related nannoplankton of the early Tertiary in alifornia. Micropaleontology. 7, 29. Debyser, J., Le Pichon,, and Montadert, L. (eds). 97. Histoire Structurale du Golfe de Gascogne, Editions Technip, Paris 2 vols. Hay, W. W. and Mohler, H. P., 967. alcareous nannoplankton from early Tertiary rocks of Pont Labau, France, and Paleocene-Early Eocene correlations, /. Paleontol. 4, 505. Helms, P. B. and iedel, W.., 97. Skeletal debris of fishes. In Initial eports of the Deep Sea Drilling Project, Volume VII. Washington (U.S. Government Printing Office.). Jones, E. J. W. and Ewing, J. I., 969. ge of the Bay of Biscay; evidence from seismic profiles and bottom samples. Science. 66,02. Jones, E. J. W. and Funnell, B. N., 968. ssociation of a deep seismic reflector and upper retaceous sediment in the Bay of Biscay. Deep-Sea es. 5, 70. Laughton,. S., 97. The Southern Labrador Sea-a key to the Mesozoic and early Tertiary evolution of the North tlantic. Nature. 232, 62. Le Borgne, E. and Le Mouel, J., 970. artographic aeromagnetique du Golfe de Gascogne... cad. Sci. Paris. 27(D), 67. Le Pichon,., Bonin, J., Francheteau, J. and Sibuet, J., 97. Une hypothese devolution tectonique du Golfe de Gascogne. Histoire structurale du Golfe de Gascogne., Paris. Le Pichon,.. Bonnin, J. and Sibuet, J.-., 970. La Faille nordpyréneenne: faille transformante liée a Foverture du Golfe de Gascogne... cad. Sci. Paris. 27, 94. Martini, 96. Nannoplankton ans dem Tertiàr und der obersten Kreide von SW-Frankreich Senckenbergiana Lethea, Vol. 42 No. /2 p. -4. Matthews, D. H. and Williams,.., 968. Linear magnetic anomalies in the Bay of Biscay: a qualitative interpretation. Earth and Planet Sci. Letters. 4, 35. Matthews, D. J., 939. Tables of the velocity of sound in pure water and sea water. Hydrographic Dept. dm. H. D Montadert, L., Damotte, B., Debyser, J., Fail, J. P., Delteil, J.. and Valery, P., 97. The continental margin in the Bay of Biscay. In I..S.U./S..O.. Working Party 3 Symposium, ambridge 970: the geology of the East tlantic ontinental Margin: 3 Europe (continued). F. M. Delaney (Ed.). Inst. Geol. Sci. ep. No. 70/5, 06 pp. Perch-Nielsen, K., 97. Einige neue occolithen aus dem Paleozàn der Bucht von Biskaya, Meddel. Dansk Geol. Foren. 20, 347. Pitman, W.. and Talwani, M., in press. Sea floor spreading in the North tlantic. Bull. Geol Soc. m. iedel, W.. and Sanfilippo,., 970. adiolaria, Leg 4, Deep Sea Drilling Project. In Bader,. G. et al, 970, Initial eports of the Deep Sea Drilling Project, Volume IV. Washington (U. S. Government Printing Office), 503., 97. enozoic adiolaria from the Western Tropical Pacific, DSDP Leg VII. In Initial eports of the Deep Sea Drilling Project, Volume VII. Washington (U. S. Government Printing Office.) Sibuet, J.. and Le Pichon,., 97. Structure gravimetrique du Golfe de Gascogne et le fosse marginal nord-espagnol. Histoire structurale du Golfe de Gascogne, Paris, 970. Sibuet, J., Pautot, G. and Le Pichon,., in press. Interpretation structurale du Golfe de Gascogne a partir des profils de sismique. Histoire structurale du Golfe de Gascogne, Paris, VI 0,. Stride,. H., urray, J.., Moore, D. G. and Belderson,. H., 969. The marine geology of the tlantic ontinental margin of Europe. Phil. Trans. oy. Soc.. 264, 3. Williams,.. and McKenzie, D., 97. The evolution of the N.E. tlantic. Nature, 232, 68. Vanney, J.., 967. La montagne sous-marine "antabria" (Golfe de Gascogne). Trav. entre. ech. d'etude Oceanographique. 7,

28 SHIPBOD SIENTIFI PTY m.y SITE 8 SITE 9 QUITINE PLEI SNDY TUBIDITES OF TEI- IE FTED DETITL MINS GENOUS DETITL MTEIL o I I V. FINE TUBIDITES. o tgiving WY TO SNDY TUBIDITES OF DETITL BONTE WITH EWOKED EOENE 00LITHS. LW. MIO. UMULTION OF PELGI SEDIMENTS WITH "TOUH OF TUBIDITE". ONTINUED UMULTION OF SHLLOW WTE, LUSTINE ND FLUVITILE SEDIMENTS HITUS IN UPLIFT OF NTBI h i 8 [M. EOENE < Q_ O en o UMULTION OF PELGI ED LYS UMULTION OF PELGI ED LYS GIVING WY TO FLOODS OF SNDY TUBIDITES OF DETITL BONTE WITH E- WOKED ETEOUS OOLITHS FUTHE UMULTION OF SHLLOW WTE BONTES. '///ETH MOVEMENTS UMULTION OF BONTE SEDS. Figure 7. Sedimentation and tectonic events at Site 8, Site 9 and in the quitaine. Data for the quitaine is taken from Bonnard et al,

29 SITE , cm PLTE , cm o Plate. Primary sedimentary structures in the turbidites, Site 9. 78

30 SHIPBOD SIENTIFI PTY PLTE 2 %tt W T *f- iu Paleocene mrbidite to P < ore 34. Hole 9), enlargement of piece and counterpiece 2 (Photos, J. v. Hinte, courtesy of Imperial Oil Enterprises, Ltd.). 782

31 SITE 9 PLTE 3 () (B) Plate 3. () Slickenslides in clayey sediment (9-37-3,5-25 cm); (B) Burrowed, convoluted fine sediment (9-37-3, cm); () Burrowed fine sediment, slightly deformed by Tectonic movement (9-37-3, 93-03). (Photos, J. v. Hinte, courtesy of Imperial Oil Enterprises, Ltd.). 783

32 -J oo PPENDI. SHIPBOD SME SLIDE OBSEVTIONS Site Hole 9 9 ore 2Section 2 Interval (cm) Sand Silt lay Quartz Feldspar Pyroxene hlorite Dark Mica Light Mica Dark Glass Light Glass Palagonite Glauconite Phosphorous Pyrite uthigenic arbonates Barite Phillipsite Other Zeolites Micronodules Other Minerals bundance Estimated arbonates Foraminifera alcareous Nannofossils Diatoms adiolaria Sponge Spicules Plant Debris Fish Debris Lithology and omments Silty clay; limonite, hornblende. Sandy silt; hornblende, limonite, zircon c c D c c c c c c c c c D D Silty clay; limonite, hornblende. Sandy silt; limonite, hornblende. Slightly sandy, silty clay; limonite. Slightly silty clay; limonite. Sandy silty clay; hornblende. Sandy silt. Silty clay. Slightly silty clay; rare limonite. Silty clay. Slightly sandy clay. Slightly silty clay; limonite. Silty clay. Sandy silt; zircon. Silty clay. lay; limonite. Silty clay; tourmaline, limonite. Silty clay; limonite. lay I D D Slightly silty clay. Silty clay. Silty clay. Silty clay. Silty clay. Silty clay. Silty clay Silty clay. D = Dominant, 65+%; = bundant, 4 65%; = ommon, 6%-40%; = are, 0%-5%.

33 PPENDI - ontinued

34 -J oo PPENDI - ontinued U oö ü lal w w ü s. i J - rt is s - rh te 3ö I I ft 8a c *5 ^ u ^ δ 8 o "cl <u S 8 * o ' 3 ^ <l PQ a N ft.h 3 <U δ 8 <u o <: III Λ O rt W PL, U.2 o.2.a S Q OJ 2 "5 o c Λ ft J2 w α. - Lithology and omments D D D D D D D D D D D D D D D D D D D D D D D D D D D D D D D D D D D D Silty clay; rare limonite. Nannoplankton-marl ooze; other minerals - limonite. Silty clay; limonite. Silty clay; limonite. Nannofossil-marl ooze; calcite or dolomite rhombs; other minerals - limonite (). Silty clay; limonite. Silty clay (nannopl. marl ooze); all glass, palagonite and quartz shows alteration rims (quartz uncertain but anisotropic with wavey extintion); many small calcite or dolomite rhombs; other minerals - limonite (). Silty nannofossil clay; many calcite or dolomite rhombs; limonite (). Nannofossil chalk ooze. Marly coccolith clay. Silty marly clay. Silty clay; quartz shows alteration rim; other minerals - limonite (). occolith marl ooze. occolith ooze. occolith chalk ooze; much recrystallized; other minerals - limonite (). ecrystallized coccolith ooze. ecrystallized coccolith ooze. ecrystallized coccolith marl. arbonate silt (recrystallized); other minerals - limonite (). occolith marl (recrystallized). ecrystallized coccolith marl.. occolith marl (recrystallized); other minerals - limonite (). ecrystallized coccolith marl; other minerals - limonite (). ecrystallized coccolith marl.

35 PPENDI - ontinued

36 SHIPBOD SIENTIFI PTY PPENDI B. GIN SIZE DETEMINTIONS ON SMPLES FOM SITE 9 Site ore Section Interval Per ent Sand Per ent Silt Per ent lay lassification Bottom Silty clay Silty clay Silty clay Silty clay Silty clay Silty clay Silty clay Silty clay Silty clay Silty clay Silty clay Silty clay Silty clay Silty clay Silty clay Silty clay Silty clay Silty clay Silty clay Silty clay Silty clay Silty clay Silty clay Silty clay lay Silty clay Silty clay Silty clay lay lay layey silt Silty clay Silty clay Silty clay Silty clay Silty clay Silty clay lay Silty clay Silty clay Silty clay lay Silty clay 'nalyses carried out under the supervision of G. W. Bode and. E. Boyce, Scripps Institution of Oceanography. 788

37 SITE 9 PPENDI. BON-BONTE ONTENT OF SMPLES FOM SITE 9 Site ore Section Top Interval Hole Depth Total arbon Organic arbon c a co nalyses carried out under the supervision of G. W. Bode and. E. Boyce, Scripps Institution of Oceanography. 789

38 SHIPBOD SIENTIFI PTY PPENDI D. LISTS OF SELETED PLNKTONI ND BENTHONI FOMINIFE ND GE DETEMINTIONS W.. Berggren Hole 9 Sample 2-9--, 4043 cm: ich planktonic foraminiferal fauna with effects of calcium carbonate solution visible. PF: Orbulina universa (dominant, abundant), Globorotalia hirsuta, G. inflata, G. truncatulinoides, G. crassaformis, Globigerina bulloides, G. pachyderma, Globigerinoides rubra. BF: Gyroidina sp., Pullenia sp., Eponides sp., milolids. lso present: elatively abundant ice-rafted quartz and other detrital rock fragments. ge: Pleistocene. Sample , cm: Lithology similar to sample above but greater predominance of coldwater species in this sample at the expense of temperate and warmwater species. PF: Globigerina bulloides (dominant, abundant), G. BF: pachyderma, Globorotalia hirsuta, G. inflata. ich and diverse, including Melonis pompilioides, Epistominella exigua, Pullenia sp., Uvigerina sp., various cibicidids. lso present: bundant ice-rafted quartz and other detritus. ge: Pleistocene. Sample 2-9-, Bottom Section 3, No ore atcher Sample: PF: Globigerina bulloides (dominant, abundant), G. pachyderma, Globorotalia hirsuta, G. inflata, G. crassaformis, G. truncatulinoides. BF: Pyrgo murrhyna, Melonis pompilioides, M. parkerae, Pullenia sp., Epistominella exigua, Eponides tener, uvigerinids, dentalinids, miliolids. lso present: elatively abundant ice-rafted quartz and other detrital rock fragments. ge: Pleistocene. Sample 2-9-2, Top: adiolaria and siliceous sponge spicules present. Planktonic foraminifera represented by scattered, broken fragments caused by solution. ge: Pleistocene (by interpolation). Sample , cm: PF: Globigerina pachyderma (dominant, abundant), G. bulloides, Orbulina universa, Globorotalia inflata, Hastigerina siphonifera. BF: Pyrgo murrhyna, Eponides sp., cibicidids, Epistominella exigua. lso present: Ice-rafted quartz. ge: Pleistocene. Sample , cm: Lithology and fauna essentially similar to above but including also Globorotalia crassaformis and Globorotalia truncatulinoides (relatively common). lso present: Ice-rafted quartz and rock fragments. ge: Pleistocene. Sample , 6-9 cm: Planktonic fauna characterized by overwhelming dominance of Globigerina pachyderma (sinistrally coiled) and minor amounts of Globigerina bulloides and Globorotalia inflata. lso present: Ice-rafted quartz. ge: Pleistocene. Sample 2-9-2, ore atcher: PF: Orbulina universa (dominant, abundant), Globigerina bulloides, G. pachyderma, Globorotalia inflata, G. crassula, G. truncatulinoides, Hastigerina siphonifera, Globigerinoides conglobata, G. rubra, Globorotalia crassaformis. BF: Pyrgo murrhyna, Eponides tener, Eggerella sp., cibicidids, miliolids. lso present: Ice-rafted quartz and other rock fragments. ge: Pleistocene. emarks: This is a calcareous ooze with varying amounts of icerafted detritus. Solution effects are visible on the tests of the planktonic foraminifera. Sample , 48-5 cm: PF: Orbulina universa, Globigerina bulloides, Globorotalia crassula, G. crassaformis, G. scitula, G. puncticulata, Globigerinoides obliqua. BF: ich and diverse, dominated by large and robust specimens of assidulina subglobosa, Pyrgo murrhyna, Melonis pompilioides, Epistominella exigua. ge: Pliocene. Sample , cm: Essentially the same fauna as above but strong effects of calcium carbonate solution visible in planktonic fauna. Globorotalia puncticulata common, and this appears to be one of the more resistant species. ge: Pliocene. Sample 2-9-3, ore atcher: PF: Orbulina universa, Globigerina bulloides, Globorotalia crassula, G. crassaformis, G. puncticulata, Globigerinoides sacculifera, G. obliqua. BF: Gyroidina spp., Laticarinina halophora, Pyrgo murrhyna, Eponides sp., Melonis pompilioides, Ehrengergina sp., Eggerella sp., Epistominella exigua. lso present: bundant pyrite clusters. ge: Pliocene. emarks: Globorotalia puncticulata occurs relatively commonly in this core and its presence together with Globigerinoides obliqua supports a Pliocene age determination for ore 3. This is also supported by the assignment of ore 3 to the Discoaster surculus Zone by K.P-N. Sample 2-94, ore atcher: PF: Orbulina universa, Globigerina praebulloides, G. atlantica, G. nepenthes, Globigerinoides sp. cf. G. canimarensis. BF: Gyroidina sp., Planulina ariminensis, Melonis pompilioides, Pyrgo murrhyna, Stilostomella abyssorum, Stilostomella spp., Eggerella sp., Pleurostomella sp. ge: Late Miocene. Sample 2-9-5, Top: PF: are, mostly dissolved. BF: Large robust, Gyroidina sp., Melonis pompilioides, Planulina driminensis, Eggerella sp., Lingulina sp., Stilostomella abyssorum, yclammina sp. lso present: bundant, very small, circular, spiney, calcareous, spheres, echinoid spines, shark teeth, and a few sponge spicules, and a few adiolaria. Similar faunas to above were found in the following samples: Sample ,28-3 cm Sample , cm Sample , cm Sample 2-9-5, ore atcher: PF: are, mostly dissolved; Globoquadrina dehiscens, Globorotalia sp. cf. G. acostaensis. BF: assidulina sp. (common), Eponides sp., Eggerella sp., Gyroidina sp., Planulina (common), siphonodosariids, Vaginulina sp., Melonis pompilioides. lso present: s above. ge:?middle Miocene (based upon calcareous nannofossils). emarks: adiolarians are relatively common in this core. The effects of solution are evident in the fact that almost all the planktonic foraminifera have been dissolved. The solution effect can also be seen on the tests of some benthonic foraminifera. The benthonic foraminiferal fauna consists wholly of abyssal forms such as Gyroidina sp., Planulina, and Melonis. 790

39 SITE 9 Sample , cm: adiolarian ooze with no planktonic foraminifera. Sample , cm: adiolarian ooze; no planktonic foraminifera. BF: Gyroidina sp., Siphonodosaria sp. Sample , cm: s above. Sample 2-9-6^, cm: Lithology essentially similar to samples above but planktonic foraminifera are also present. PF: Globorotalia peripheroronda, G. siakensis, Globorotalia sp. cf. G. praescitula, Globoquadrina dehiscens. BF: s above. ge: Early-Middle Miocene. Sample 2-9-6, ore atcher: adiolarian ooze with moderate planktonic and benthonic foraminiferal fauna. PF: Globigerinita dissimilis, G. unicava, Globoquadrina praedehiscens, G. dehiscens, G. baroemoenensis, Globigerinoides sp. cf. G. diminuta, Globorotalia siakensis. BF: nomalinoides pompilioides,. semicribrata, ibicidoides trincherasensis,. grimsdalei, Gyroidina sp., Stilostomella spp. Vulvulina sp. ge: Early Miocene (Zone N6). emarks: ore 6 contains the highest occurrence at this site of Globigerinita dissimilis and G. unicava and several benthonic forms which are characteristic of the aribbean region. Specimens referred here to Globorotalia siakensis have a distinct loop-shaped aperture and bear a strong resemblance to Globorotalia semivera Jenkins described from the Lower Miocene of the quitaine Basin. Sample , cm: adiolarian ooze, few calcareous benthonic foraminifera, no planktonic foraminifera. BF: nomalinoides semicribrata, assidulina sp., Oridorsalis ecuadorensis. ge: Early Miocene (see below). Sample , cm: Essentially same as above. Large dentalinids present. ge: Early Miocene. Sample , cm: Essentially the same as above. Some foraminifera preserved, including Globoquadrina dehiscens. ge: Early Miocene. Sample 2-9-7, ore atcher: adiolarian ooze with moderate benthonic and planktonic fauna. PF: Globigerinita dissimilis, G. unicava, Globoquadrina praedehiscens, G. dehiscens. BF: ibicidoides trincherasensis,. grimsdalei, Stilostomella spp., nomalinoides semicribrata, Gyroidina complanata, G. girardana. ge: Early Miocene. emarks: The planktonic and benthonic foraminiferal fauna of ore 7 is essentially the same as that occurring in ore 6. Sample , cm: adiolarian ooze with few scattered broken fragments of planktonic and benthonic foraminifera. BF: nomalinoides pompilioides,. semicribrata, stilostomellids, assidulina subglobosa, Gyroidina complanata. ge: Early Miocene. Sample , cm: Essentially the same as preceding sample above. Sample , cm: Greenish-gray clay with abundant adiolaria, no calcareous fauna preserved. Sample , Top: Lithology same as preceding sample above. Sample , cm: Lithology same as above but with some planktonic foraminiferal elements {Globorotalia inflata, orbulinids) and benthonic foraminifera from higher levels representing contamination. Sample 2-9-8, ore atcher: Benthonic and planktonic foraminifera as described from ores 6 and 7 above, but including also Pliocene-Pleistocene planktonic and benthonic foraminiferal contaminants from above, such as Orbulina universa, Globorotalia crassula, G. puncticulata, Globigerina bulloides, G. pachyderma, Melonis pompilioides, etc. emarks: Quartz grains are relatively abundant in the fine fraction in samples in ore 8, with the exception of the ore atcher sample for reasons difficult to explain. Section 5 and the ore atcher were found to contain contaminants from Pliocene/ Pleistocene levels above. Sample , 48-5 cm: adiolarian ooze with few fragments of calcareous benthonic forms: primarily fragments of Ellipsonodosaria, Gyroidina and Eponides. Sample , cm: adiolarian ooze with few fragments of calcareous benthonic forms; gyroidinids primarily. Sample , cm: Essentially the same as preceding sample above. Sample 2-9-9, ore atcher: adiolarian ooze, with rare planktonic foraminifera. BF: assidulina subglobosa, Pullenia sp., nomalinoides semicribrata, ibicidoides trincherasensis, Vulvulina sp., Gyroidina spp., siphonodosariids, Stilostomella spp. ge: Early Miocene (by interpolation). Sample , cm: adiolarian ooze, no observable calcareous fauna preserved. Sample , cm: Lithology same as above, few gyroidinids, cassidulinids. Sample , 6-9 cm: Same as above. Sample 2-9-0, ore atcher: adiolarian ooze with sparse planktonic and benthonic fauna. PF: Globigerinita dissimilis (very rare). BF: Siphonodosariids, Vulvulina sp., Gyroidina sp.,planulina renzi, Melonis sp., Eponides sp., Karreriella sp., assidulina subglobosa, Oolina sp. ge: Late Oligocene or Early Miocene. emarks: ore 0 is a radiolarian ooze in which the calcareous foraminifera are present in rare to moderate numbers. Quartz occurs commonly in the fine fraction. Sample 2-9--, cm: adiolarian ooze with few foraminiferal fragments preserved. Sample , cm: adiolarian ooze with abundant siliceous sponge spicules and few scattered benthonic foraminifera (Gyroidina, Pullenia, Siphonodosaria, Stilostomella). Sample , cm: Lithology and fauna essentially the same as above. Sample 2-9-, ore atcher: adiolarian ooze with moderate benthonic foraminiferal fauna, planktonic foraminifera rare. PF: Globigerinita unicava, Globigerina sp. BF: Gyroidina sp., nomalinoides semicribrata, Karreriella sp., Vulvulina sp., ibicidoides trincherasensis, Planulina sp., siphonodosariids. lso present: Some contaminants from Pliocene to Pleistocene ge: (planktonic foraminifera). Late Oligocene to Early Miocene (calcareous nannoplankton). emarks: ore consists of radiolarian ooze with a moderate benthonic foraminiferal fauna. Quartz is a common component in 79

40 SHIPBOD SIENTIFI PTY the fine fraction. In the absence of diagnostic planktonic foraminifera age determination is based on calcareous nannoplankton. Sample , cm: adiolarian ooze with abundant siliceous sponge spicules and scattered benthonic foraminifera. Sample , 48-5 cm: adiolarian ooze with abundant sponge spicules and benthonic and planktonic foraminifera. PF: Globigerinita unicava, Globigerina sp. BF: Gyroidina, assidulina, ibicidoides, Vulvulina, Karreriella, Stilostomella, Siphonodosaria. ge: Late Oligocene (calcareous nannoplankton). Sample , cm: PF: Globigerinita dissimilis, G. unicava, Globorotalia opima nana, G, siakensis. BF: Karreriella sp.,ellipsonodosariasp.,ngulogerinasp., Gyroidina sp. ge: Late Oligocene. Sample 2-9-2, ore atcher: adiolarian ooze with moderate benthonic and rare planktonic foraminifer al fauna. PF: Globigerinita unicava, G. dissimilis, Globorotalia opima nana, BF: ibicidoides sp. (with central umbilical plug), assidulina sp., Gyroidina sp., Eponides sp., Planulina sp. ge: Late Oligocene (calcareous nannoplankton). emarks: s in the case of cores above, ore 2 is composed of radiolarian ooze in which most of the calcareous foraminiferal fauna has been dissolved. Quartz and mica flakes are abundant in the fine fraction. Sample , cm: Buff-colored calcareous ooze with abundant radiolarian and sponge spicules. PF: BF: ge: Globigerinita unicava, G. dissimilis Gyroidina sp., assidulina sp., Siphonodosaria sp., Karreriella sp., Pleurostomella sp., Stilostomella sp., ibicidoides sp. Late Oligocene (calcareous Nannoplankton). Sample , cm: Lithology and fauna as above. Sample , cm: Lithology as above. Sample 2-9-3, ore atcher: Tan calcareous ooze with abundant radiolarian and sponge spicules. bundant quartz and mica in the fine fraction. PF: are, including Globigerinita dissimilis and G. unicava. BF: Gyroidina complanata, G. girardana, assidulina subglobosa (common), Oridorsalis ecuadorensis, ibicidoides sp. ge: Late Oligocene (calcareous nannoplankton). Sample , cm: alcareous ooze; residue of abundant quartz in the fine fraction; foraminifera rare. {Gyroidina sp., Pleurostomella sp., assidulina sp., Oridorsalis ecuadorensis, ibicidoides spρ.) lso present: bundant sponge spicules. ge: Late Oligocene (calcareous nannoplankton). Sample , 48-5 cm: alcareous ooze with abundant quartz in fine fraction. Foraminifera rare {Gyroidina sp., Pleurostomella sp., assidulina sp.), scattered small planktonic foraminifera. Sample , cm: Lithology and fauna essentially the same above, including Globigerinita unicava and G. dissimilis. alcareous foraminifera strongly recrystallized. bundant quartz in fine fraction. Sample 2-9-4, ore atcher: alcareous ooze, strongly recrystallized with a rich planktonic foraminiferal fauna. Most of the planktonic foraminifera exhibits varying degrees of dissolution, ranging from partial to extreme. PF: Globigerinita dissimilis, G. unicava (abundant), hiloguembelina (rare), Globigerina tripartita, Globorotalia opima, small nonkeeled globorotaliids. BF: Siphonodosaria spp., Gyroidina sp., Planulina sp., Melonis sp., Karreriella sp., Vulvulina sp., Oridorsalis ecuadorensis, Lenticulina sp., nomalinoides semicribrata, assidulina subglobosa. ge: Late Oligocene (Zone P2). emarks: The occurrence together of Globorotalia opima and hiloguembelina in the ore atcher sample suggests that this part of ore 4 (at least) is within the lower part of Zone P2. This agrees well with the assignment of the lower part of ore 4 to the Sphenolithus distentus Zone by K.P-N. Sample , cm: Tan calcareous marl with abundant quartz in fine fraction. adiolarians and sponge spicules also present in the fine fraction. Scattered small benthonic foraminifera, (gyroidinids, stilostomellids, ellipsonodosariids, Pullenia, ibicidoides, cassidulinids) and various planktonic foraminifera (globigerinitids, too small for identification). Sample , cm: Tan calcareous marl with abundant quartz in fine fraction. adiolarians and sponge spicules also present in fine fraction. Scattered small benthonic foraminifera (gyroidinids, stilostomellids, siphonodosariids, cassidulinids) and planktonic (globigerinitids) fauna. Sample , cm: Lithology and fauna essentially the same as preceding samples above. ge: Late Oligocene (calcareous nannofossils). Sample , 49-5 cm: Lithology and fauna essentially the same as preceding samples above including ibicidoides grimsdalei. Sample , cm: Lithology and fauna essentially the same as above, including various agglutinated genera such as Karreriella sp. and Vulvulina sp. Sample 2-9-5, ore atcher: Tan calcareous marl with abundant quartz in pan fraction. PF: Globigerinita dissimilis, G. unicava, Globorotalia opima nana, Globigerina tripartita, G. selli, Globorotaloides suteri. BF: Gyroidina sp., Siphonodosaria sp., Oridorsalis ecuadorensis, Textilaria sp., Vulvulina sp.,nomalinoides semicribrata, Pleurostomella sp., assidulina sp. ge: Late Oligocene (calcareous nannofossils). emarks: Planktonic and benthonic foraminifera are relatively abundant in ore 5. Globigerinitids are the dominant planktonic foraminiferal element. Specimens exhibit evidence of recrystallization. Quartz and mica are abundant in the fine fraction. Sample , cm: PF: Globigerinita dissimilis, G. unicava, Globorotalia opima nana, Globorotalia opima. BF: ibicidoides spp., assidulina sp. ge: Late Oligocene (Zone P2). Sample , 9-2 cm: Lithology and fauna essentially the same except a large number of agglutinated forms assignable to Bathysiphon and Hyperammina. Gyroidinids, pleurostomellids and siphonodosariids common. Quartz and mica very abundant in fine fraction. ge: Late Oligocene (Zone P2). Sample , cm: Lithology and fauna essentially as preceding sample above. BF: ibicidoides havanensis, Ellipsoglandulina multicostata, Gyroidina girardana, Pleurostomella sp., Nodosarella sp., and agglutinated forms as indicated above. ge: Late Oligocene (Zone P2). Sample , 3-34 cm: Lithology and fauna as above. ge: Late Oligocene (Zone P2). 792

41 SITE 9 Sample 2-9-6, ore atcher: PF: Globigerinita dissimilis, G. unicava, Globorotaloides suteri, Globorotalia opima nana. BF: elatively rich and diverse, including among others, ibicidoides grimsdalei, Vulvulina jan>isi, Dorothia brevis, Ellipsoglandulina sp., nomalina alazanensis, Gyroidina girardana, nomalinoides semicribrata. ge: Late Oligocene (Zone P2). emarks: ore 6 contains a relatively rich and diverse benthonic foraminiferal fauna. Quartz (in an aggregate form) and mica are abundant in the fine fraction. Sample , cm: PF: Globigerinita dissimilis, G. unicava, Globorotalia opima nana, Globorotaloides suteri. BF: elatively rich and diverse as in ore 6 above. ge: Early-Late Oligocene. Sample , 50-5 cm: Lithology and fauna essentially the same as above. Globorotalia opima nana particularly abundant in this sample. BF: ich and diverse, including among others, Oridorsalis ecuadorensis, ibicidoides grimsdalei, Gyroidina girardana, Vulvulina jarvisi, Stilostomella spp., Pleurostomella spp., Nodosarella spp. ge: Early-Late Oligocene. Sample , cm: Lithology and fauna essentially the same as above, including Nodosarella mappa. ge: Early-Late Oligocene. Sample , cm: Lithology and fauna as above. ge: Early-Late Oligocene. Sample 2-9-7, ore atcher: PF: BF: ge: Globigerinita dissimilis, G. unicava, opima nana, Globorotaloides suteri. Globorotalia ich and diverse, including among others, Stilostomella verneuili, Stilostomella subspinosa, Nodosarella subnodosa, Siphogenerina sp., ibicidoides grimsdalei, Oridorsalis ecuadorensis, Karreriella sp., Vulvulina jarvisi. Early-Late Oligocene (?//. reticulata Zone, according to calcareous nannoplankton). emarks: ore 7 contains a rich and diverse benthonic foraminiferal fauna, and a relatively low diversity planktonic foraminiferal fauna in which Globorotalia opima nana is the dominant form. Quartz and mica are abundant in the fine fraction, often in aggregate form. Sample , cm: PF: Globigerinita dissimilis, G. unicava, Globorotalia opima nana. BF: elatively diverse but present primarily in fine fraction. Specimens too small for identification. ge: Early Oligocene (calcareous nannoplankton). Sample , cm: Fauna and lithology essentially as in sample above. Benthonic fauna includes, ibicidoides grimsdalei, Oridorsalis ecuadorensis, Karreriella sp., various stilostomellids. ge: Early Oligocene, Sample , cm: Lithology and fauna essentially as above. ge: Early Oligocene. Sample , cm: Lithology and fauna essentially as above. Many specimens show effects of solution. ge: Early Oligocene. Sample , cm: Lithology and fauna as above. ge: Early Oligocene. Sample , cm: Lithology and fauna as above. ge: Early Oligocene. Sample 2-9-8, ore atcher: PF: Planktonic foraminifera extremely rare. Present primarily in the pan fraction; globigerinitids. BF: ich and diverse, well-preserved benthonic foraminiferal fauna, including among others, ibicidoides grimsdalei, Oridorsalis ecuadorensis, Stilostomella abyssorum, Vulvulina jarvisi, Ellipsodimorphina subcompacta, Gyroidina octocamerata, Gyroidina perampla, nomalina alazanensis, ibicidoides martinizensis, Ellipsoglandulina sp., Ellipsoglandulina multicostata, Stilostomella subspinosa, Stilostomella verneuili. ge: Early Oligocene. Sample , 6-8 cm: Essentially unfossiliferous. few fish fragments and teeth and a residue of black elongate (? manganese) fragments. Sample cm: Small residue, consisting of agglutinated foraminifera, ibicidoides havanensis, Gyroidina sp., Bulimina sp. cf. B. grata, Globigerina sp. cf. G. linaperta. ge: Eocene. Sample , cm: esidue confined mostly to small fraction. few larger agglutinated forms in coarser fraction. Fauna consists of various benthonic foraminifera including Nuttallides truempyi, Bulimina grata, various cibicidids and chiloguembelinids. Sample 2-9-9, ore atcher: esidue of fine particulate carbonate matter. adiolaria, sponge spicules and diverse benthonic foraminiferal fauna. PF: are, including Globigerinita sp., Globorotalia centralis. BF: Nuttallides truempyi, Nodosarella subnodosa, nomalinoides sp. ge: Middle Eocene. emarks: ore 9 contains a relatively diverse benthonic foraminiferal fauna but most elements are confined to the finer fractions and/or broken rendering specific determination difficult. The presence of Nuttallides truempyi and Bulimina grata indicate an Eocene age for ore 9, and the presence in the ore atcher of Globorotalia centralis confirms this determination. Sample , cm: Foraminiferal fauna confined essentially to the fine fraction and containing, among other forms, Nuttallides truempyi, ibicidoides trinitatensis (=. tuxpamensis). ge: Middle Eocene. Sample , cm: Lithology and fauna essentially the same as sample above. Sample , cm: elatively rich benthonic foraminiferal fauna, including among others, labamina dissonata, Nuttallides truempyi, Bulimina grata, Ellipsodimorphina subcompacta, Dorothia sp. carinina coalingensis, (=. triplex =. primitiva) also observed. ge: Middle Eocene. Sample , cm: Lithology and fauna essentially the same as sample above. Sample , ore atcher: BF: ibicidoides trinitatensis, labamina dissonata, Nuttallides truempyi, Dorothia sp., Gaudryina sp., Oridorsalis ecuadorensis, Bulimina grata, Karreriella sp., Ellipsodimorphina subcompacta. emarks: ore 20 is characterized by relatively diverse benthonic foraminiferal fauna, in which the dominant and characteristic elements are Nuttallides truempyi, labamina dissonata, and Bulimina grata. Planktonic foraminifera are essentially absent from the samples in this core, probably owing to the effects of solution. 793

42 SHIPBOD SIENTIFI PTY Sample , cm: PF: are (Probably owing to the effects of calcium carbonate solution); Globigerina senni. BF: Nuttallides truempyi, labamina dissonata, Oridorsalis ecuadorensis, Bulimina grata. ge: Middle Eocene. Sample , cm: elatively diverse benthonic foraminiferal fauna consisting of, among others: Nuttallides truempyi, labamina dissonata, Bulimina grata, assidulina sp., Pullenia sp., Gaudryina sp., Dorothia sp., Gyroidina sp. ge: Middle Eocene. Sample , cm: Lithology and age essentially the same as sample above. Sample , cm: Lithology and fauna essentially the same as above. Fish bones and teeth abundant. ge: Middle Eocene. Sample 2-9-2, ore atcher: PF: BF: Not observed. elatively diverse and well-preserved benthonic fauna, consisting of Eponides truempyi, labamina dissonata, Vulvulina sp., Stilostomella gracillima, Stilostomella abyssorum, Gaudryina sp., Nodosarella sp., Nodosarella mappa, Vulvulina jarvisi, Dorothia sp., Plectina cubensis, Bathysiphon sp., ibicidoides trinitatensis Karreriella sp., Eggerella sp. ge: Middle Eocene. emarks: s in ores 9 and 20, this core is characterized by rich and well-preserved benthonic foraminiferal fauna dominated by Eponides truempyi and labamina dissonata. Planktonic foraminifera are absent, probably owing to the effects of solution. Sample , cm: PF: Not observed. BF: Nuttallides truempyi, ragonia sp., labamina dissonata. ge: Middle Eocene. Sample , ore atcher: PF: Globigerina senni, carinina coalingensis. BF: Nuttallides truempyi, ibicidoides havanensis, Bathysiphon irregularis, Nodosarella sp., ibicidoides trinitatensis, Dorothia sp., Gaudryina sp., Bulimina grata. lso present: bundant shark teeth. ge: Middle Eocene. emarks: The lithology and fauna of ore 22 is essentially the same as the cores immediately above. Data from the calcareous nannoplankton suggest that ores 9 through 22 are, in fact, of approximately the same age, that is, assignable to the same calcareous nannoplankton zone. Sample , ore atcher: esidue consisting primarily of fine quartz and mica and fragments of a black mineral with red-brown oxidized coating and abundant shark teeth. No planktonic foraminifera observed. Benthonic fauna contains Eponides truempyi, Verneuilina sp. and various small, mostly broken fragments. ge: Early Eocene (calcareous nannoplankton). emarks: Only the ore atcher sample was studied from ore 23. Planktonic foraminifera are absent from this sample and the benthonic foraminifera are confined primarily to the very fine fraction. Sample , cm: esidue of fine quartz, mica and abundant shark teeth. Benthonic foraminifera rare, indeterminable. Sample , cm: Lithology and fauna same as preceding sample above. Sample , ore atcher: Quartz residue with rare benthonic foraminiferal fauna consisting of agglutinated forms assignable to Gaudryina sp. and Dorothia sp. Shark teeth also present. ge: Basal part of Early Eocene (according to calcareous nannoplankton). emarks: ore 24 contains a very small and relatively poorly preserved benthonic foraminiferal fauna. This core would appear to contain the upper limit of the thick turbidite section developed in ores 25 to 40 below. Sample , cm: Sample essentially barren of foraminifera. Sample , cm: esidue of abundant, but extremely small, planktonic foraminifera, primarily species of Globigerina, Globorotalia (G. subbotinae) and acarininids. ge: Late Paleocene (calcareous nannoplankton). Sample , cm: Planktonic foraminifera rare and poorly preserved. esidue of quartz sand (in aggregate form) and mica and sparse planktonic foraminiferal fauna. PF: Globigerina triangularis, G. velascoensis, Globorotalia aequa, Globorotalia pasionensis, carinina coalingensis. ge: Late Paleocene. Sample , 4-44 cm: esidue of fine sand and abundant adiolaria. Planktonic foraminifera very rare, primarily small globigerinids and acarininids. Sample , cm: esidue of fine sand and abundant adiolaria. Planktonic foraminifera rare, primarily small globorotaliids and acarininids and globigerinids. Sample , ore atcher: Quartz sand residue with no determinable foraminiferal elements. Foraminifera essentially restricted to pan fraction. hert, chalk and manganese fragments observed. emarks: ore 26 consists primarily of sand- and silt-sized fragments in aggregate form with a poor foraminiferal fauna. The sediments are of turbidite origin. Sample , cm: Data as above. Sample , ore atcher: Quartz residue with rare planktonic foraminifera, primarily confined to the pan fraction. PF: Globigerina velascoensis, carinina esnaensis. BF: Virtually absent. Sample , cm: Quartz residue with rare planktonic foraminifera, with the exception of chiloguembelinids, which are relatively common but poorly preserved. Sample , ore atcher: Essentially barren. Large silt-sand fraction and abundant recrystallized radiolarians. No age determination possible in ore. 28. Sample , cm: Foraminifera rare, re crystallized adiolaria abundant. Sample , cm: Essentially barren. Sample , cm: Foraminifera extremely rare. esidue consists of essentially silicified adiolaria (abundant). Sample , cm: esidue of silicified adiolaria (abundant) and planktonic foraminifera (keeled globorotaliids and acarininids). Poor preservation makes specific identification impossible'. Sample , ore atcher: Quartz sand in aggregate form of turbidite origin. bundant extremely small recrystallized planktonic and benthonic foraminifera in the pan fraction. Planktonic forms include keeled globorotaliids of the acuta-velascoensis group. Benthonic forms include Bolivina, Melonis, and Discorbis types, as well as nodosariids. hiloguembelinids relatively common also. ge: Late Paleocene. 794

43 SITE 9 Sample , 0-7 cm: Quartz sand residue with abundant and poorly preserved adiolaria; planktonic foraminifera present, but in general poorly preserved. PF: carinina soldadoensis, Globigerina triangularis, Globorotalia ex gr. acuta-velascoensis. ge: Late Paleocene. Sample ,45-48 cm: Quartz sand residue with abundant mica and extremely small specimens of chiloguembelinids, globigerinids, and acarininids. Sample , cm: Quartz sand residue with abundant but poorly preserved chiloguembelinids and small globigerinids. Sample , ore atcher: Fine silty recrystallized fragments and adiolaria. Foraminifera extremely rare. single specimen of a keeled globorotaliid (velascoensis type) observed. Sample , cm: esidue of quartz sand, mica and small poorly preserved chiloguembelinids, acarininids, globigerinids and bolivinids. Sample , cm: esidue of aggregate quartz silt and mica. Foraminifera rare and poorly preserved, primarily acarininids and chiloguembelinids. Sample ,92-95 cm: Lithology and fauna essentially as in preceding sample above. Sample , cm: esidue of quartz silt with abundant mica and relatively common carbonaceous fragments; foraminifera rare and poorly preserved (recrystallized). Sample , ore atcher: Foraminifera rare, including Globigerina triloculinoides, G. triangularis. BF: Eponides?, Pullenia, Osangularia. ge: Paleocene. emarks: The presence of Globigerina triloculinoides in the ore atcher of sample suggests that this core is no younger than mid- Paleocene (Zone P4). This is supported by the assignment of ore 32 to the Heliolithus kleinpelli Zone. Sample , ore atcher: Hard quartz silt and mica. Barren of foraminifera. Sample , ore atcher: esidue of quartz grains, mica, manganese nodules, echinoid fragments. Essentially barren of foraminifera. Sample , cm: Small residue of quartz silt and silicified adiolaria. Sample , ore atcher: Hard, very fine-grained siltsone. Barren of foraminifera. Sample , 3-6 cm: esidue of quartz silt; planktonic foraminifera rare (keeled globorotaliids and chiloguembelinids). ge: Late Paleocene. Sample , cm: Gray siltstone with few specimens of adiolaria present.essentially barren of foraminifera. Sample , cm: Gray siltstone with small fauna of poorly preserved globigerinids. Sample , ore atcher: Gray siltstone, essentially barren of foraminifera. Sample , cm: esidue of very small planktonic foraminifera (globigerinids and globorotaliids) and mica, with moderate amounts of carbonaceous material. ge: Late Paleocene. Sample , cm: Silty, sandy quartz fragments; white chalky marl fragments; essentially barren of foraminifera. Sample , ore atcher: Silty, sandy, quartz fragments, white chalky marl fragments, essentially barren of foraminifera. Sample , 20-2 cm: ecrystallized carbonate and quartz residue with few planktonic foraminifera in fine fraction (compressed globigerinids and nonkeeled globorotaliids and chiloguembelinids). ge: Late Paleocene. Sample , Top Section 4: Quartz residue with a few planktonic foraminifera: Globigerina triloculinoides, chiloguembelinids, small compressed globorotaliids similar to G. imitata. ge: Late Paleocene. Sample , cm: ecrystallized carbonate and quartz residue; essentially barren of foraminifera. Sample , ore atcher: halky sediment with moderate planktonic foraminiferal fauna. PF: Globorotalia pseudobulloides, G. varianta, G. angulata, G. conicotruncata, G. ehrenbergi, Globigerina trilocu linoides. BF: are and extremely small, indeterminable. ge: Late Paleocene (Zone P3, G. pusilla-angulata), probably upper part. emarks: The presence of Globorotalia angulata and conicotruncata in ore 38 provides one of the few reference points in the sequence of Paleocene cores from 24 to 40. The occurrence of these two forms together indicate that ore 38 is of early Late Paleocene age and this is confirmed by the assignment of the upper part of ore 38 to the Fasciculithus tympaniformis Zone and the lower part to the Ellipsolithus macellus Zone (calcareous nannoplankton zonation). Sample , 6-20 cm: halky, marly sediment with small and poorly preserved planktonic foraminiferal fauna. PF: Globigerina triloculinoides, Globorotalia pseudobulloides, G. varianta, G. ex gr. compressa-ehrenbergi. Sample , cm: halky, marly sediment. Barren of foraminifera. Sample , -6 cm: halky, marly sediment with small foraminiferal fauna. PF: Minute globigerinids and non-keeled globorotaliids, specifically indeterminate. BF: mmodiscus sp. Sample , cm: Lithology and fauna essentially the same as preceding sample above. Sample , ore atcher: halky, marly sediment with small planktonic foraminiferal fauna in pan fraction. PF: ge: hiloguembelinids, Globigerina triloculinoides, Globorotalia pseudobulloides, small keeled globorotaliids (? angulata) and smooth 3 and 4-chambered forms. Basal part Late Paleocene (post Danian). Sample , 0-4 cm: halky, recrystallized residue; essentially barren of foraminifera. Sample , 04 cm: halky, recrystallized residue with rich planktonic foraminiferal fauna. PF: Globigerina triloculinoides, G. spiralis, Globorotalia pseudobulloides, G. compressa, G. angulata. ge: Earliest Late Paleocene. emarks: The association of Globigerina spiralis and Globorotalia angulata in ore 40 indicates that the oldest sediments cored at this site are of earliest Late Paleocene age and referable to the top of Zone P2 or the base of Zone P3. 795

44 SHIPBOD SIENTIFI PTY Hole 9 PPENDI E. OOLITH SPEIES ND STTIGPHI SSIGNMENT OF SITE 9 David Bukry Upper Pleistocene , cm; depth 2 m: occolithus pelagicus, yclococcolithina leptopora, Gephyrocapsa spp., Helicopontosphaera kamptneri. eworked Upper retaceous taxa: hiastozygus disgregatus (Stover), retarhabdus crenulatus, Prediscosphaera cretacea cretacea. Middle Miocene (Discoaster exilis Zone) , cm; depth 99 m: occolithus eopelagicus, yclococcolithina leptopora, Discoaster exilis, Discoaster subsurculus Gartner, Helicopontosphaera granulata, H. kamptneri, eticulofenestra pseudoumbilica, Sphenolithus neoabies, Triquetrorhabdulus rugosus. Middle Oligocene (Sphenolithus distentus Zone) , cm; depth 38 m: hiasmolithus altus, occolithus eopelagicus,. fenestratus, yclococcolithina neogammation, Dictyococcites abisectus, D. bisectus, D. scrippsae, Discoaster deflandrei, eticulofenestra gartneri, Sphenolithus distentus (Martini), S. moriformis, S. predistentus. eworked retaceous taxon: retarhabdus crenulatus. Lower Oligocene (Helicopontosphaera reticulata Zone) , cm; depth 353 m: hiasmolithus altus,. oamaruensis, occolithus eopelagicus,. fenestratus, yclococcolithina neogammation, Dictyococcites bisectus, D. scrippsae, Discoaster deflandrei, D. tani nodifer, D. tani tani Bramlette and iedel, Helicopontosphaera compacta, Isthmolithus recurvus, eticulofenestra hillae,. umbilica,?habdosphaera tenuis [stems]. Middle Eocene (hiphragmalithus quadratus Zone) , 40-4 cm; depth 357 m: ampylosphaera dela, hiasmolithus gigas,. grandis, hiphragmalithus mexicanus (Stradner),. sp. cf.. spinosus (Stradner), yclococcolithina formosa, Discoaster barbadiensis, D. martinii Stradner, D. saipanensis, D, tani nodifer, D. wemmelensis, eticulofenestra samodurovi Middle Eocene (Discoaster sublodoensis Zone) , cm; depth 375 m: hiasmolithus grandis, hiphragmalithus cristatus, occolithus pseudogammation,. staurion, Discoaster barbadiensis, D. mirus Stradner, D, sublodoensis, D. wemmelensis, habdosphaera inflata, Sphenolithus radians, Triquetrorhabdulus inversus. Lower Eocene (Discoaster lodoensis Zone) , cm: depth 380 m: occolithus sp. [rim fragments resulting from solution], Discoaster barbadiensis, D. lodoensis, D. nonaradiatus, D. septemradiatus (klumpp), Discoasteroides kuepperi. Lower Eocene (Tribrachiatus orthostylus Zone) , 4-42 cm; depth 392 m: occolithus sp. [rare rim fragment], Discoaster barbadiensis, D. lodoensis, D. nonaradiatus [rare], Discoasteroides kuepperi, Tribrachiatus orthostylus [abundant, late variety]. Series unknown , 2-22 cm; depth 40 m: Barren , cm; depth 402 m: Barren , cm; depth 402 m: Barren. Upper Paleocene (Discoaster multiradiatus Zone) , cm; depth 420 m: Braarudosphaera bigelowi, ampylosphaera eodela, hiasmolithus bidens,. californicus (Sullivan), consuetus, Discoaster delicatus Bramlette and Sullivan, D. falcatus Bramlette and Sullivan, D. helianthus Bramlette and Sullivan, D. limbatus Bramlette and Sullivan, D. multiradiatus, Discolithina plana, D. Solida (Deflandre), Ellipsolithus distichus, Fasciculithus involutus Bramlette and Sullivan, F. schaubi Hay and Mohler, Scapholithus apertus Hay and Mohler, Toweius eminens, Zygodiscus plectopons Bramlette and Sullivan, Z. sigmoides Bramlette and Sullivan, Zygolithus chiastus Bramlette and Sullivan, Z. distentus Bramlette and Sullivan, Z. junctus Bramlette and Sullivan, Zygrhablithus bijugatus, Z. simplex Bramlette and Sullivan. The preservation and diversity of this assemblage matches that of the lower Lodo Formation in alifornia (Bramlette and Sullivan, 96). eworked Upper retaceous taxa: rkhangelskiella cymbiformis, Prediscosphaera cretacea cretacea, Zygodiscus deflandrei Bukry. Upper Paleocene (Discoaster mohleri Zone) , cm; depth 500 m: Braarudosphaera bigelowi, hiasmolithus bidens,. californicus,. consuetus, occolithus pelagicus s. I, Discoaster mohleri Bukry and Percival, Discoasteroides megastypus Bramlette and Sullivan, Ellipsolithus distichus, E. macellus, Fasciculithus tympaniformis, Heliolithus kleinpellii, H. riedelii Bramlette and Sullivan, Scapholithus apertus, Toweius eminens, Zygodiscus plectopons, Zygolithus chiastus. eworked Upper retaceous taxa: Broinsonia parca, Watznaueria barnesae. Upper Paleocene (Heliolithus kleinpellii Zone) , cm; depth 544 m: hiasmolithus sp. cf.. bidens,. consuetus, ruciplacolithus tenuis (Stradner), yclolithella sp. cf.. robusta (Bramlette and Sullivan), Ellipsolithus macellus, Fasciculithus involutus, F. tympaniformis, Heliolithus kleinpellii, H. riedelii [rare], Toweius eminens, Zygodiscus sp. aff. Z. plectopons Bramlette and Sullivan, Z. sigmoides, Zygolithus chiastus. eworked Upper retaceous taxa: Broinsonia parca, Micula decussata, Watznaueria barnesae. Lower Paleocene (ruciplacolithus tenuis Zone) , 5-56 cm; depth 704 m: Braarudosphaera bigelowi, occolithus pelagicus s.l., ruciplacolithus tenuis, Ericsonia? subpertusa Hay and Mohler, Zygodiscus sigmoides. eworked Upper retaceous taxa: Prediscosphaera cretacea cretacea, Watznaueria barnesae. 796

45

46 SHIPBOD SIENTIFI PTY HOLE 9 OE SEDIMENT DENSITY! gm cm J OMPESSIONL WVE VELOITY PENETO METE WTE ONTENT (wt.) POOSITY (vol.) f km sec" I0" 2 cm % P I I I I I I GIN SIZE % by wt. LY SILT SND ao3 %by NTUL GMM DITION t I0 3 counts/7.6 cm/75 sec J I I I I I I t djusted data, see hapter 2 798

47 SITE 9 HOLE 9 0 TO 9 OE LITHOL. LITHOLOGY DIGNOSTI FOSSILS BIO- STT. TIME STT. EMPTY EMPTY M T Soft Foram-nannofossil mud foram nannofossi mud, gray and grayish orange. oarse fraction mineral grains and forams. Soft, disrupted silty clay. Flora: ooaolithus petagicus, yoloaocaolithus leptoporus, Helieopontosphaera kamptnerz, Syr>acosphaera sp., Gephyrocapsa aperta, G. cf. oeeaniaa plus reworked retaceous coccoliths: Predisaosphaera aretaaea, Microrhabdulus decoratus, Watznaueria barnesae Forams: G. hirsuta, G. inflata, G. arasβaformis G. pachyderma, G. bulloides Flora similar to above, plus Eeliaopontosphaera sellii; no reworked coccoliths Flora similar to above, plus reworked Tertiary coccomths~.oaaol ithus eopelagious \Λ Soft silty ooze, coarse fraction practically all forams. Flora similar to Sect ray Mineralogy (Bulk) 5Y 6/ alc. Dolo. Qtz. Plag. Kaol. Mica hi. Mont. morph Flora similar to above, reworked Tertiary coccoliths Foram fauna as above ore atcher: Flora similar to above, plus reworked retaceous and Tertiary coccoliths 799

48 SHIPBOD SIENTIFI PTY HOLE 9 OE 2 SEDIMENT DENSITY t gm cm r T OMPESSIONL WVE VELOITY km sec~' PENETO METE l<t 2 cm P00 0 i i WTE ONTENT (wt.) POOSITY (vol.) f I I I I GIN SIZE ao. % by wt. LY SILT SND NTUL GMM DITION t I0 3 counts/7.6 cm/75 sec J l I I i t djusted data, see hapter 2 800

49 SITE 9 HOLE OE TO 59 LITHOL. LITHOLOGY DIGNOSTI FOSSILS BIO STT. TIME STT. EMPTY N,M F 5Y 5/3 5Y 6/2 5Y 6/3 5Y 7/ -ray Mineralogy (Bulk) alc. Qtz Plag. Kaol. Mica hi. morph Soft, olive silty clay much disturbed by flow-in. oarse fraction is a mixture of mineral grains, forams and rock fragments. Pyritized worm burrow at 48 cm in Sec. 2. Forams: β, paahyderma, G. bulloides, G. inflat<zj Hast, siphonifera Only small coccoliths. Flora: yaloaooaolithus leptoporus, "oβaolithus jaramillensis", Saapholithus fossilis, Syraaosphaera sp., Ponto- sphaera discopora, Heliaopontosphaera kamptnerij H. sellii, Pseudoemiliania laaunosa Flora similar to above Foratn fauna as above; G. paahyderma (abund.) Flora similar to above M ompletely mud. disrupted soft -ray Mineralogy (Bulk) EMPTY alc. Qtz. Kaol. Mica morph Flora poorer than above Olive gray and light gray silty clay. Flora similar to.above, plus habdosphaera alavigera cc ore atcher: Foram fauna as above. Flora similar to above, plus few oaaolithus pelagiaus No radiolarians 80

50 SHIPBOD SIENTIFI PTY HOLE 9 OE 3 SEDIMENT DENSITY t gm cm OMPESSIONL WVE VELOITY km sec ' 2.0 PENETO METE I0" 2 cm PIOO I0 I I WTE ONTENT (wt.) POOSITY (vol.) t GIN SIZE ao } % by wt. % by LY SILT SND wt 54 NTUL GMM DITION t I0 3 counts/7.6 cm/75 sec J I i i i i t djusted data, see hapter 2 HOLE 9 OE 4 SEDIMENT DENSITYt gm cm OMPESSIONL WVE VELOITY km sec" PENETO METE I0T 2 cm PIOO 0 [ I WTE ONTENT (wt) POOSITY (vol ) t I I I I GIN SIZE % by wt. LY SILT SND ao, % by NTUL GMM DITION t I0 3 couπts/7.6 cm/75 sec J J J I I I I I t djusted data, see hapter 2 802

51 SITE 9 HOLE 9 OE 3 00 TO 09, LITHOLOGY DIGNOSTI FOSSILS BIO- STT. TIME STT. Disturbed gray and very light gray soft nannofossil ooze. oarse fraction consists of broken and corroded forams and a few fish teeth. Yellowish gray, soft nannofossil ooze. -ray Mineralogy (Bulk) alc. Qtz. Kaol. Mica Flora: Disooastev brouweri, Disaoaster suraulus, Heliσopontosphaera kamptneri, H. sellii, habdolithus sp., Pseudoemiliania laaunosa, Syracosphaera sp. Pontosphaeva disoopora, Thoracosphaera sp., Flora: oaaolithus pelagians, yctococcolithus leptoporus,. maaintyrei, plus few reworked coccoliths Forams: G. bulloides, G. crassula, G. arassaisj G. soitula, G. punotioutata, Flora similar to above Foram fauna as above; strong solution effects ore atcher: No radiolarians Flora similar to above Foram fauna as above. HOLE H OE 4 LITHOL. LITHOLOGY DIGNOSTI FOSSILS BIO- STT. TIME STT. EMPTY M Light olive gray dense nannofossil clay, mottled with medium bluish gray (5B 5/). oarse fraction is broken and corroded forams and a few mineral grains. -ray Mineralogy (Bulk) Flora: Disaoastex var>iábil ùs_, D. ahalzengevi_, D. cf. bollii, ooaotithus petagicus, yolocooaolithus leptoporus,. maβintyrei, etiaulofenestra pseudowribilioa, üelieopontosphaera kamptneri alc. Qtz. Kaol. Mica morph Flora similar to above, plus Tx iquetrorhabdulus rugosus Forams: Globigerina atlantlaa, G. nepenthes, G. praebultoides, G. cf. eanimarensis cc ore atcher: Flora similar to above, plus few reworked coccoliths (Eocene and retaceous). No radiolarians. 803

52 SHIPBOD SIENTIFI PTY HOLE 9 OE 5 to ETE I 2 Z o O Q 4 SEDIMENT DENSITYt gm cm" I J J j f / OMPESSIONL WVE VELOITY km sec ' PENETO METE I0" 2 cm P00 0 WTE ONTENT (wt.) POOSITY (vol.) t % J* < GIN SIZE % by wt. LY SILT SND ao 3 %by wt. πy NTUL GMM DITION t I0 3 counts/7.6 cm/75 sec \J_ I _) J _ 3 3 > - < 3 t I j """5! -< -j S \ {s - i i i i i +djusted data, see hapter 2 804

53 SITE 9 HOLE 9 OE 5 98 TO 207 LITHOL. LITHOLOGY DIGNOSTI FOSSILS BIO- STT. TIME STT. _LT N - -5B F, N, M F N 8/ Light greenish gray firm 7/ nannofossil clay with light bluish gray bands as indicated. Yellowish gray mottled at 3-8 cm in Sec.l and cm in Sec. 2. oarse fraction is forams and foram fragments. alc. Qtz. Kao!. Mica Mont. morph. Mineralogy (Bulk) Foram fauna mostly dissolved Flora: ocoolithus pelagious;. eopelagiaus_, yclocoocoli thus leptoporus, eticulofenestva pseudoimbilica> Discoaster exilis, D. deflandrei, D. extensus, Sphenolitkus sp., yaloaoaoolithus neogarrmat ion,. macintyvei Forams as above adiolarians yery rare. Digitately branched Oroscena spines. Flora similar to above adiolarians same Forams as above. Flora similar to above. adiolarians rare, as above. Forams as above. ore atcher: adiolarians common. Digitately branched Orosoena spines, yrtooapsella tetraperaj. gaponioa, aiocyolas margatensis. Flora similar to above. Forams rare, mostly dissolved; Gl. dehiseens, Gl. cf. aoostaensis 805

54 SHIPBOD SIENTIFI PTY HOLE 9 OE 6 SEDIMENT DENSITY! gm cm" T r OMPESSIONL WVE VELOITY km sec ' PENETO METE lot 2 cm PIOO 0 I WTE ONTENT (wt.) POOSITY (vol ) t % a c0 3 GIN SIZE % by wt. % by wt LY SILT SND NTUL GMM DITION t I0 3 counts/7.6 cm/75 sec I I i 8 + djusted data, see hapter 2 j I 806

55 SITE 9 HOLE OE TO 249 m METES _ _ _ - _ - _ SETION LITHOL. >- i Q_ LU s: -~ ~-~J. T ~_~_ JT_~_~_T _._ -_ _... LT _~_T:_ "~ r_~_"~_" ~-~~-~~-~ ~_~-~-~- SMPLES N F N M F N F D l\ N F._ F ~-~--. N ^_ >- LO -σ 5Y 4/ <> >- LD -çj O >- ir> -σ <o LO O >- > s. 5Y 6/, 5G 6/ 5Y 8/ LITHOLOGY Light olive αrav and olive gray dense silty clay mottled with medium bluish gray. Some yellowish gray clay in Sec. 3. -ray Minerai alc. Qtz. Kaol. Mica Mont. morph DIGNOSTI FOSSILS Flora: Disaoaster deflandrei, Disaoaster cf. aulakos, D. ahallengeri, oaaolithus pelagiaus,. eopelagious, oronoayalus niteseens, Sphenolithus heteromorphus, etioulofenestra pseudoumbilica, yoloooocolithus neogammation No Foraminifera. adiolarians abundant. aloayaletta costata,. virginis, Stiohooorys armata, S. wolffii, S. delmontensis, yalampterium (?) leptetrum, yrtooapsella japoniaa,. aornuta,. tetrapera, Lyahnooanium bipes, annartus tubarius, alooyolas margatensis Flora similar to above adiolarians abundant as above plus Doroadospyris simplex, annartus prismaticus, arpoaanopsis aingulatum No planktonic forams; Gyroidina, Siphonodosaria present adiolarians common, similar to above plus annartus violina, less aloayoletta aostata Flora similar to above Foram fauna as above adiolarians abundant, similar to above plus arpoaanopsis bramlettei Flora similar to above Forams: G. peripheroronda, G. siákensis, G. cf. praesoitula, Gl. dehisoens ore atcher: Forams: Gl. dissimilis, G. uniaava, Gl. praedéhisoens, G. dehisoens, G. baroemoenensis, Gl. siákensis Flora similar to above plus Heliaopontosphaera ampliaperta adiolarians very abundant, similar assemblage plus arpoaanopsis favosum stat BIO- STT. α oleti s> o ts 5 -S 3 -to. -W 03 o t-i cδ 3 O -2 +i *i < Qi & a. gni r ü, to +i So TIME STT. LU z o Σ. >- <: LU 807

56 SHIPBOD SIENTIFI PTY HOLE 9 OE 7 SEDIMENT DENSITY! gm cm OMPESSIONL WVE VELOITY km sec~' PENETO METE 0T 2 cm P00 0 I I WTE ONTENT (wt.) POOSITY (vol.) t % a 3 GIN SIZE % by wt. % by LY SILT SND wt NTUL GMM DITION t I0 3 counts/7.6 cm/75 sec t djusted data, see hapter 2 J I I I I I 808

57 I i SITE 9 HOLE 9 OE 9 METE _ - - _ I 2 -J _ 3 - _ SETI LITHOL. : :. II I I l l l l II I I : I I I I I I I I _. i i i i MM I I I I ' i' i i' i' i' i i i MM ' I I I I SMPL N F N VM F N F N c 249 TO 258 LITHOLOGY 5Y 8/ Yellowish gray dense clay with with light bluish gray and greenish 5B 7/ gray mottled. and 5G 6/ 5Y 7/2 passing down into light gray dense clay with light bluish gray and greenish gray mottles and greenish gray bands. -ray Mineralogy (Bulk) alc. 37. Qt Plag..4 Kaol 7 4 5G 6/ ' Mica 3.0 by " ù Mont G 6/ morph Y 7/2 DIGNOSTI FOSSILS adiolarians common. yrtooapsella japoniaa,. oornuta,. tetrapera, alooyoletta virginis, Stichooorys delmontensis, S. diplooonus, S. wolffii, Doroadospyris simplex, Lyohnoaanium bipesj arpooanopsis oingulatum Flora: ocaolithus pelagicus,. eopelagiaus, yoloaocaolithus neogamnation, Discoaster deflandrei, Triquetrorhabdulus aarinatus, oronooyolus nitescens, Sphenolithus moriformis, S. belermos, Helioopontosphaera kamptneri, etiaulofenestra pseudoumbiliaa No planktonic forams Flora similar to above adiolarians abundant. Same assemblage plus yolampterium (?) leptetrum, annartus tubarius,. prismatious, alocyalas margatensis, arpooanopsis braxnlettei Foram fauna as above Flora similar to above adiolarians common. Same assemblage. Foram fauna mostly dissolved; Gl. dehisoens (rare) ore atcher: adiolarians very abundant. Same assemblage plus annartus viouna and one aloayoletta oostata (contaminant?) Flora similar to above Forams: G. dissimilis, G. unicava, G. praedehisoens, G. dehisoens BIO- STT. IL ^ o Λ Iirg O K o c- TIME STT. LU LU HO >- ac LU 809

58 SHIPBOD SIENTIFI PTY HOLE 9 OE 8 SEDIMENT DENSITYt gm cm OMPESSIONL WVE VELOITY km sec~ PENETO METE I0" 2 cm WTE ONTENT (wt.) POOSITY (vol ) t PI T T I I % GIN SIZE % by wl. LY SILT SND ao, %by 9 NTUL GMM DITION t 0' counts/7.6 cm/75 sec J I I I I I I I + djusted data, see hapter 2 80

59 SITE 9 HOLE 9 258TO 267 OE 8 LITHOL. LITHOLOGY DIGNOSTI FOSSILS BIO- STT. TIME STT..M N 5Y 8/ 5G 6/ 5G 4/ 5GY 8/ 5G 6/ i 5G 5/ adiolarians abundant, Same assemblage as ore 7. Flora: ocβolithus pelagians 3. eopelagiaus, yoloaocaolithus neogammation, etiaulofenestra paeudoumbitiaa^ Disβoaster deflandrei, D. druggi, Triquetrorhabdulus aarinatus, Sphenolithus belermos, oronooyalus nitesaens Planktonic forams mostly dissolved. N M N M N F M O D ^5G 6/ 5G 8/ 5G 4/ ' 9/?G^ 5G 4/ FY 6/ 5G\ 9/ 5Y 6/ á 9/ 5GY 4/ F N.F N 5G 5/ Firm, \lard greenish gray nannofossil clay, almost an ooze. Highly burrowed throughout. -ray Mineralogy (Bulk) alc 24.2 Qtz. 9.0 Plag 2. Kao! 6.5 Mica 38.6 Mont 9.6 morph adiolarians abundant. Similar to above plus yalamptex>ium (?) pegetrium. Flora similar to above Flora similar to above adiolarians abundant. Similar assemblage plus Dorcadospyris ateuehus. Foram fauna as above Flora similar to above adiolarians abundant. Similar assemblage plus annartus violina, yalampterium (?) sp. cf.. (?) milowi Foram fauna as above No coccoliths No coccoliths : Foram fauna as above (plus Pleist. contaminants) adiolarians common, similar to above. ore atcher: Dark: Flora similar to above Light: Flora similar to above Foram fauna as above plus Pleistocene contaminants adiolarians very abundant, similar to above. Possible downhole contamination indicated by very rare specimens of Lithopera renzae and aloayoletta costata 8

60 SHIPBOD SIENTIFI PTY HOLE 9 OE 9 SEDIMENT DENSITYt gm cm OMPESSIONL WVE VELOITY km sec~' PENETO METE I0" 2 cm P00 0 WTE ONTENT (wt.) POOSITY (vol.) t % GIN SIZE ao. % by wt. % b LY SILT SND w( NTUL GMM DITION t I0 3 counts/7.6 cm/75 sec [ I I I s 56 + djusted data, see hapter 2 J I 82

61 SITE 9 HOLE OE jo 276 LITHOL. LITHOLOGY DIGNOSTI FOSSILS BIO- STT. TIME STT. cc N M,M 5G 4/ 5G 9/ 5Y 6/ 5Y 8/ 5B 5/ 5B 7/ -ray Mineralogy (Bulk) alc. 5.5 Qtz Plag. 3.8 Kaol 6.9 Mica 35.2 Mont. 4.4 morph Mottled and disturbed greenish gray clay. t Darker t Dark green-gray clay Lighter t Mottled light olive gray clay Yellowish and bluish gray clay Slickensides on two perpendicular planes at 05 cm in Sec. 2. Firm greenish gray and light olive gray clay Slickenside at 00 cm in Sec. 3. -ray Mineralogy (Bulk) alc. Qtz. Plag. Kaol. Mica Mont. morph Flora: oaaolithus pelagians,. eopelagicus, yolococcolithus neogammation> eticülofenestva pseudownbiliβa, Discoaster deflandrei, Triqnetrorhábdulus carinatus No foram fauna adiolarians rare. Dorcadospyris simplex D. ateuehua, Stiahoaorys delmontensis t yx>tocapsella japonica,. oovnuta,. tetr>apera, (?) aloayaletta virginis, yclamptevivm (?) sp. cf.. (?) rrrilowi,. (?) pegetrium, Lychnocanium bipes, annartus pvismatious, alocyclas margatensis Flora similar to above, plus reworked Eocene No planktonic forams; rare benthonics Flora similar to above, plus reworked Eocene adiolarians rare, similar assemblage. ore atcher: adiolarians abundant, similar assemblage plus yclampteriion (?) leptetrum and yrtocapsella elongata. Minor contamination from up the hole. Flora similar to above Planktonic foram fauna sparse; nom. semicribrata, ib. trinchevasensis, stilostomellids 83

62 SHIPBOD SIENTIFI PTY HOLE 9 OE 0 SEDIMENT DENSITY t gm cm OMPESSIONL WVE VELOITY km sec ' PENETO METE I0" 2 cm P00 0 WTE ONTENT (wt.) POOSITY (vol.) t % GIN SIZE ao, % by wt. LY SILT SND NTUL GMM DITION t I0 3 counts/7.6 cm/75 sec J j J I I I I I + djusted data, see hapter 2 84

63 SITE 9 HOLE TO 284 OE LITHOL. LITHOLOGY DIGNOSTI FOSSILS BIO- STT. TIME STT. M N M.F N M F N,F 5B 7/ 5Y 5/3 M Mineralogy (Bulk) Firm, highly mottled nannofossil ooze, yellowish-gray and light olive gray. oarse fraction is sponge spicules, forams, radiolarians, mineral grains and fish debris. Highly distrubed -ray Mineralogy (Bulk) (277.5 i neters) alc. 52. Qtz. 9.7 Kaol. 5.0 Mica 30. Mont. 3.2 morph ray Mineralogy (Bulk) (278.5 meters) alc Qtz. 3.4 Plag..6 Kaol. 5.0 Mica 29.8 Mont. 6.7 morph adiolarians rare. ssemblage similar to ore 9. Flora: oaβolithus petagieus,. eopetagicus, yclococcolithus neogcarnation, etiaulofenestra pseudoiσribiliaa, Sphenolithus moriformis, Tviquevovhabdulus aarinatus, Disaoaster deflandrei No forams Flora similar to above adiolarians rare, similar to above. Benthonic forams only Flora similar to above adiolarians rare, similar to above. ompletely disrupted nannofossil ooze cc adiolarians very abundant, assemblage similar to ore 9. Minor contamination from up the hole. Flora similar to above Forams sparse; G. dissimilis 85

64 SHIPBOD SIENTIFI PTY HOLE 9 OE SEDIMENT DENSlTYt gm cm J OMPESSONL WVE VELOITY km sec PENETO METE!0" 2 cm S PI00 I0 WTE ONTENT (wt.) POOSITY (vol.) t % I \r! a GIN SIZE 0 3 % by wt. % by LV SILT SND wt NTUL GMM DITION t I0 3 counts/7.6 cm/75 sec I I I I I I + djusted data, see hapter 2 86

65 SITE 9 HOLE 9 OE 284 TO 293 LITHOL. LITHOLOGY DIGNOSTI FOSSILS BIO- STT. TIME STT. 2 M N 5B 9/ I- 5B 9/ Firm yellow-gray and gray, slightly mottled nannofossil ooze. -ray Mineralogy (Bulk) alc. Qtz. Kaol. Mica Mont. morph adiolarians common. yvtooapsella aornuta,. tetrapeva, Voraadospyris simplex, D. ateuahus^ (?) Stiahoaovys delmontensis, (?) S. wolffii 3 (?) S. diplooonus, Lyehnocanium bipes, yolampterium (?) pegetrwn,. (?)sp. cf., (?) milow i, annartus prismatiausj Theoayrtis annosa, Theocoryβ spongooonvm, arpoaanopsis aingulatum Flora: oaaolithus pel igicus,. eopelagicus, etiaulofenestra pseudoumbiliea, yoloaooaolithus neogcomation, oaoolithus cf. biseotus, Sphenolithus moriformis, S. belemnos, Discoaster deflandrei, Triquetrorhabdulus aarinatus Few foram fragments Flora similar to above adiolarians very rare. yolampterium (?) sp. cf.. (?) milowi. bove species absent. Flora similar to above Scattered benthonic forams: Gyvoidina, pullenia, Siphonodosaria s Stilostomella Flora similar to above adiolarians same as above. Forams fauna as above Disrupted ompletely disrupted pale yellow and light bluish gray nannofossil clay cc bundant contaminant radiolarians from the. virginis zone above. dark: Flora similar to above light: Flora similar to above Forams: Globigerinita dissimilis, G. uniaava 87

66 SHIPBOD SIENTIFI PTY HOLE 9 OE 2 5 SEDIMENT DENSITY t gm cm J OMPESSIONL WVE VELOITY km sec PENETO METE I0"" cm PI00 I0 I T T WTE ONTENT (wt.) POOSITY (vol.)t % GIN SIZE LY SILT SND a c 3 NTUL GMM DITION + I0 counts/7.6 cm/75 sec 0 K djusted data, see hapter 2 J I 88

67 SITE 9 HOLE 9 OE 2 293x0 302 LITHOL. LITHOLOGY DIGNOSTI FOSSILS BIO STT. TIME STT. M N F Flora: ocoolithus pelagicus>. eopelagiaus 3. aff. biseotus,. biseatus> Sphenolithus moriformis, Sphenolithus sp., ycloeoσaolithus neogammation_, Discoastev deftandrei_, Triquetvorhabdulus aarinatus adiolarians very rare. yalampteriwn (?) sp. cf.. (?) milowi, orosphaerids Scattered, small benthonic forams cc N, N.M N _5B 7/ Pale yellow and white or light bluish gray, slightly mottled, hard, firm nannofossil ooze -ray Mineralogy (Bulk) alc. Qtz. Plag. Kao!. Mica Mont. morph Flora similar to above adiolarians the same. Forams: Globigerinita unicava Flora similar to above Flora similar to above adiolarians very rare. (?) yi>tocapsella tetvapeva, aloayolas margatensisj orosphaerids. Forams: G. dissimilis, G. unicava, G. opi ma nana s G. siákensis ore atcher: few contaminant radiolarians from above. Flora similar to above. Foram fauna as above. 89

68 SHIPBOD SIENTIFI PTY HOLE 9 OE 3 is SEDIMENT DENSITY t gm cm OMPESSIONL WVE VELOITY km sec~ PENETO METE I0-2 cm PIOO 0 i r WTE ONTENT (wt.) POOSITY (vol.) f % i i r GIN SIZE % by wt. ao, % by LY SILT SND NTUL GMM DITION t I0 3 counts/7.6 cm/75 sec " OH + djusted data, see hapter 2 j L 820

69 SITE 9 HOLE 9 OE TO 3 LITHOL. LITHOLOGY DIGNOSTI FOSSILS BIO- STT. TIME STT. N F, N Flora: ooootithus pelagiaus,. eope~lagicus }. biseotus,. aff. biseatus, yalooooaolithus neogamnat ion, Sphenolithus moriformis, Sphenolithus sp., Disaoaster deflandrei Forams: G. dissimilis, G. unicava No radiolarians Flora similar to above 2 few zeolitized spumellarians. M 3." Dense, pale yellow nannoooze. oarse fossil fraction is sponge spicules forams,, fish debris and mineral grains. -ray Mineralogy (Bulk) alc Qtz. 6. Kaol..8 Mica.9 lin..2 morph Foram fauna as above FJora similar to above plus Triquetrorhabdutus oarinatus few zeolitized radiolarians. One contaminant. tetrapera Flora similar to Sect N M Flora similar to above No radiolarians. - ore atcher: Very rare contaminant radiolarians from the. viz>ginis zone above. Flora similar to Sect Foram Fauna as above. 82

70 SHIPBOD SIENTIFI PTY HOLE 9 OE 4 SEDIMENT DENSITYt gm cm OMPESSIONL WVE VELOITY km sec"' PENETO METE I0" 2 cm WTE ONTENT (wt.) POOSITY (vol.) f % PI00 I0 I T I I I I GIN SIZE * c0 3 % by wt. % by LY SILT SND wl. NTUL GMM DITION t 0"' counts/7.6 cm/75 sec 0!.O \ t djusted data, see hapter 2 j I 822

71 SITE 9 HOLE H9 3 TO 320 m OE 4 LITHOL. LITHOLOGY DIGNOSTI FOSSILS BIO STT. TIME STT. EMPTY -L. N,M Flora: oacolithus pelagicus,. eopelagicus,. bisectus,. aff. bisectus, yclococcolithus neogarmation, Triquetrorhabdulus cayvnatus> Sphenolithus mor iformis, Sphenolithus sp., Disaoaster deflandrei No radiolarians Forams: Gyrcidina, Pleurostomella, Oridorsalis ecuadovensis N M n F M N M Λ_6/3 and " 5Y 7/3 Pale yellow and pale olive, dense, firm nannofossil clay, slightly mottled very pale blue (5B 8/2). oarse fraction contains abundant mineral grains. -ray Mineralogy (Bulk) alc. Qtz. Kaol. Mica lin. morph Flora similar to above, less Triquetrorhabdulus carinatus Very rare zeolitized radiolarians. Flora similar to Sect. 2 plus reworked retaceous: rkhangelskiella oymbiformis No radiolarians Flora similar to above plus Triquetrorhabdulus carinatus Foram fauna as above Flora similar to above, less T. carinatus, plus Sphenolithus distentus Very rare contaminant radiolarians from the. virginis zone above. Flora similar to Sect M NM 5B 8/2 Flora similar to Sect. 4-35, plus oronocyclus nitescens y eticulofenestra laevis, Discolithina sp. Flora similar to Sect cc ore atcher: Very rare contaminants from the. virginis zone above Flora similar to Sect. 5-47, plus hiasmolithus sp. Forams: G. dissimilis, G. unicava, hiloquerribelinai &h. opima, G. tripartita 823

72 SHIPBOD SIENTIFI PTY HOLE 9 OE 5 SEDIMENT DENSITY! gm cm" OMPESSIONL WVE VELOITY km sec~ PENETO- METE 0T 2 cm P00 0 I I WTE ONTENT (wt.) POOSITY (vol.) t % GIN SIZ " 0 3 % by wt. % by LY SILT SND wt 70 NTUL GMM DITION t I0 3 counts/7.6 cm/75 sec i j I l l I i t djusted dat», see hapter 2 824

73 SITE 9 HOLE TO 329 m OE 5 LITHOLOGY DIGNOSTI FOSSILS -ray Mineralogy (Bulk) alc. 8.0 Qtz. 5.9 Kaol..6 Mica 9.9 lin..6 morph Flora: occolithus pelagicus,. eopelagicus,. bisectus,. aff. bisectus, yclococcolithus neogammation, Sphenolithus sp. S. distentus, Discoaster deflandrei, eticulofenestra laevis Scattered in determinate forams. Firm, uniform, slightly mottled pale yellow nanno fossil clay with bands of white and bluish white. oarse fraction contains abundant mineral grains, forams and mica flakes. Flora similar to above, plus Triquetrorhabdulus cf. carinatus Flora similar to Sect Flora similar to above, plus Sphenolithus cf. predistentus, hiasmolithus sp. Flora similar to Sect. 4- Very abundant zeolitized radiolarians. Foram fauna as above Flora similar to Sect. 4- Flora similar to Sect. 4- Flora similar to Sect. 4- Flora similar to Sect. 4- Foram fauna as above I gray: Flora similar to Sect. 4- cream: Flora similar to Sect. 4- Foram fauna as above plus G. sellii, G. suteri Zeolitized radiolarians very rare. ommon contaminant radiolarians from the. virginis zone above. 825

74 SHIPBOD SIENTIFI PTY HOLE 9 OE 6 SEDIMENT DENSITYt gm cm OMPESSIONL WVE VELOITY km sec"' PENETO METE I0" 2 cm PIO0 I0 WTE ONTENT (wt.) POOSITY (vol.) t % T r GIN SIZE * c 3 % by wt. % by LV SILT SND wt NTUL GMM DITION t IO J counts/7.6 cm/75 sec t djusted data, see hapter 2 J I I I i i 826

75 SITE 9 HOLE OE TO 338 m LITHOL. LITHOLOGY DIGNOSTI FOSSILS BIO STT. TIME STT. N M F N N F 0Y 7/4 N9 -ray Mineralogy (Bulk) alc. Qtz. Kaol. Mica lin. morph Pale yellow to pale olive hard, uniform nannofossil clay, slightly mottled. White layers as indicated. oarse fraction includes abundant mineral grains, sponge spicules, fish debris and some forams. Flora: oceolithus biseotus,. aff. biseotus 3 yolococoolithus neogarmation, Sphenolithus sp., S. predistentus } Disaoaster deflandrei Forams: G. dissimilis, G. unioava, G. opima, G. opima nana Flora similar to above, plus oceolithus pelagians Flora similar to above Foram fauna as above plus abundant Bahtysiphon and üyperammina Zeolitized radiolarians common. few Lower Miocene contaminants. :h i -J N Flora similar to above, plus oceolithus pelagians,. eopelagious M 5Y 8/ o Foram fauna as above o LU Flora similar to above 5Y 8/ Flora similar to above, plus hiasmolithus sp. Foram fauna as above cc ore atcher: Zeolitized radiolarians, very rare. Very rare contaminants from. virginis zone above. Flora similar to above. Forams: G. dissimilis> G. unicava 3 G. suteri, G. opima nana 827

76 SHIPBOD SIENTIFI PTY HOLE 9 OE 7 METES - SETION DISTUB LOG SEDIMENT DENSITY t gm cm" OMPESSIONL WVE VELOITY km sec PENETO METE T 2 cm PI00 0 WTE ONTENT (wt.) POOSITY (vol.) t % GIN SIZE % by wt. ao3 %by LY SILT SND NTUL GMM DITION t I0 3 counts/7.6 cm/75 sec , 2-2 _ 3 - I : e \ i 4 á ] \ \ 7 _ 5 \ 8 6 till I t djusted data, see hapter 2 828

77 SITE 9 HOLE TO 347 m OE 7 LITHOLOGY DIGNOSTI FOSSILS Flora: occolithus pelagicus,. bisectus,. aff. bisectus,. eopelagicus, yclococcolithus neogammation, eticulofenestra laevis, habdolithus sp. Sphenolithus sp. S. predistentus, Discoaster deflandrei, D. tani ornatus Silicified radiolarians very rare. Flora similar to above adiolarians same. Pale yellow and pale olive nannofossil clay with light bluish gray bands. Section is burrowed and mottled. -ray Mineralogy (Bulk) alc Qtz.. Kaol. 2. Mica 8.4 lin. 2.9 morph Flora similar to above, plus hiasmolithus sp. Forams: G. dissimilis, G. unicava, G. opima nana, G. suteri adiolarians same. Flora similar to above, plus reworked retaceous coccoliths Forams as above; G. opima nana abundant Dense pale yellow and pale olive nannofossil clay, slightly mottled with light bluish gray. Flora similar to above No radiolarians Foram fauna as above Flora similar to above No radiolarians. Flora similar to above, plus eticulofenestra umbilica Foram fauna as above ore atcher: No radiolarians. Flora similar to above, plus eticulofenestra umbilica Forams: G. dissimilis, G. unieava, G. opima nana, G. suteri

78 SHIPBOD SIENTIFI PTY HOLE 9 OE 8 GQ (J i/3 J 3.0 SEDIMENT DENSITYt gm cm" OMPESSIONL WVE VELOITY km sec ' PENETO METE I0" 2 cm PI00 0 WTE ONTENT <wt ) POOSITY (vol.) t % i r I I i! I GIN SIZE % by wl. ao3 % by LY SILT SND NTUL GMM DITION t 0* counts/7.6 cm/75 sec " t djusted d ta. see hapter 2 J I 830

79 SITE 9 HOLE OE TO 356, LITHOL. LITHOLOGY DIGNOSTI FOSSILS BIO- STT. TIME STT. Pale yellow, dense, nannofossil clay, highly burrowed, some mottling in pale blue (5PB 7/2). -ray Mineralogy (Bulk) alc. Qtz. Kaol. Mica lin. morph Flora: Isthmolithus recurvus, oacolithus eç>pelagicus,. bisectus,. aff. bisectus, yoloooaaolithus neogammation, Disaoaster deflandrei, hiasmolithus sp., Sphenolithus sp., S. predistentus, Discoaster barbadiensis (reworked?) No Identifiable radio!arians Flora similar to above, plus Disaoaster tani, etioulofenestra umbiliaa Forams: G. dissimilis, G. unicava, G. opima nana Flora similar to above, less D. barbadiensis, plus etioulofenestra wribilica No identifiable radiolarians Flora similar to above, plus Ericsonia obrutam, Neoaoacolithes sp., Disaoaster tani, less D. barbadiensis Flora similar to Sect. 2-68, plus hiasmolithus oamaruensis, Markalius inversus Foram fauna as above; ib. grimsdalei, oridorsalis eauadorensis Flora similar to Sect. 2-68, plus eticulofenestra umbilica No identifiable radiolarians Flora similar to Sect Foram fauna as above N M F N N N White and pale yellow clay, some burrowing, becoming less noticeable downwards. oarse fraction is forams and fish debris, some mineral grains. Flora similar to Sect. 3-4 No identifiable radiolarians Flora similar to Sect Foram fauna as above Flora similar to Sect. 3-4, plus Discoaster saipanensis_, Ericsonia alternans, Helicopontosphaera sp. Flora similar to Sect. 3-4, plus Ericsonia alternans Very rare silicified spumellarians. Flora similar to Sect Foram fauna as above M N _F N F Flora similar to Sect. 5-70, plus reworked retaceous {ribrosphaerella ehrenbergi), plus Zygrhablithus bijugatus, habdolithus tenuis No radiolarians Flora similar to Sect Foram fauna as above. ' few silicified radiolarians. Flora similar to Sect Forams: Planktonics rare; BF: ib.grimsdaleij Orid. ecuadorensis, ib. martinizensis, Stilostomellids, nom. alazanensis, gyroidinids 83

80 SHIPBOD SIENTIFI PTY HOLE 9 OE 9 SEDIMENT DENSITY t gm cm I 3 I OMPESSONL WVE VELOITY km see* 2.0 PENETO METE I0" 2 cm P00 0 WTE ONTENT (wt.) POOSITY (vol.) f % i r Ti T I GIN SIZE % by wt. LY SILT SND ao, NTUL GMM DITION t I0 3 counts/7.6 cm/75 sec ^ + djusted data, see hapter 2 I I I I I 832

81 SITE 9 HOLE TO 365 OE 9 LITHOL. LITHOLOGY DIGNOSTI FOSSILS BIO- STT. TIME STT. N,F goo Dense gray brown clay with some swirls, mottles and bands of pale yellow, some black mottles. Highly burrowed No coccoliths Foram fauna barren Flora: Disooaster barbadiensis y Disaoaster sp. Nannotetrina pappi > N. oristata, eticulofenestr>a wnbilioa, Eriosonia ovalis, hiasmolithus sp., Disooaster tani, D. wermelensis Flora similar to above, plus oooolithus eopelagious, hiasmolithus californicus gglutinated forams plus gyroidinids Flora similar to above Silicified and zeolitized radiolarians rare passing into Flora similar to above, plus Eviosonia alternana Forams: Nuttallides truempyi, Bui. grata Flora similar to above, plus Sphenolithus sp., hiasmolithus oalifornious N.M light brown gray and gray brown clay with interbedded lumps of white and gray. These could be contaminants Flora similar to Sect Zeolitized radiolarians common. -ray Mineralogy (Bulk) alc. Qtz. Kaol. Mica Mont. lin. morph Foram fauna as above cc Gray brown and light brown clay with pebbles of gray and white clay--probably cavings samples by lifting bit off bottom and putting it down again. 'Zeolitized radiolarians abundant. Very abundant contaminant radiolarians from the. Virginia zone above. Flora similar to Sect Forams: Globigerinitids, Gl. oentrαtis, Nuttallides truempyi } Nodosarella subnodosa 833

82 SHIPBOD SIENTIFI PTY HOLE 9 OE 20 SEDIMENT DENSITY t gm cm OMPESSIONL WVE VELOITY km sec"' PENETO METE I0T 2 cm P00 0 I T I WTE ONTENT <wt) POOSITY (vol ) t Q! I I I GIN SIZE ao3 % by wt. % by LY SILT SND NTUL GMM DITION t I0"' counts/7.6 cm/75 sec J I I I I i t djusted data, see hapter 2 834

83 SITE 9 HOLE OE TO 374 LITHOL. LITHOLOGY DIGNOSTI FOSSILS BIO- STT. TIME STT. M N,F Dense grayish brown clay with swirls, mottling and bands of white, black, and gray. Black appears only as mottles in the gray brown clay. Gray brown clay thoroughly burrowed while white clays are not. Flora; Ericsonia ovalis, E. alternans, Nannotetrina oristata, Disaoaster barbadiensis, D. saipanensis, Sphenolithus sp. oaoolithus eopelagicus, hiasmotithus califovniaus 3 hiasmolithus sp. Flora similar to above, plus Nannotetrina fulgens Zeolitized radiolarians common. Flora similar to above Forams Nuttallides truempyi, ib. trinitatensis Flora similar to above cc F,M \J 2.5Y 8/2 olor banded, dense brown 2.5Y 5/2 si it y clay 2.5Y8/2 r2.5y 5/2 2.5Y 8/2 = 2.5Y 5/2 Last 50 cm highly disturbed. -ray Mineralogy (Bulk) alc. Qtz. Kaol. Mica Paly. lin. morph Flora similar to above Foram fauna as above Flora similar to above Zeolitized radiolarians very rare. few contaminants from the. vivg inis zone Flora similar to above Flora similar to above, Neogene contamination? and reworked retaceous coccoliths [Micula staux>ophora) Foram fauna as above plus lbamina dissonata, Bui. grata, carinina aoalingensis ore atcher: Forajηs: ib. trinitatensisj lab. dissonata> Nuttallides truempyi, Oridorsalis eouadovensis 835

84 SHIPBOD SIENTIFI PTY HOLE 9 OE 2 SEDIMENT DENSITYt gm cm OMPESSIONL WVE VELOITY km sec ' PENETO METE I0" 2 cm WTE ONTENT (wt.) POOSITY (vol.) f a c0 GIN SIZE 3 % by wt. % by LY SILT SND wt "49" 7 29 NTUL GMM DITION t I0 3 counts/7.6 cm/75 sec j I I I I I I I + djusted data, see hapter 2 836

85 SITE 9 HOLE TO 383m OE 2 LITHOL. LITHOLOGY DIGNOSTI FOSSILS BIO- STT. TIME STT. N M N, M 2_.5Y 5/2 lternating layers of very pale brown and grayish brown OY 8/3' iarc '' ^ e n s e c^ay P a^e brown ' areas only slightly burrowed, gray-brown areas thoroughly 2.5Y5/2burrowed. oarse fraction is forams and fish debris. 0Y 8/ Very pale brown, burrowed clay -ray Mineralogy (Bulk) alc. Qtz. Plag. Kaol. Mica Mont. Paly morph K5Y 8/4 w h U e t Q y e o w b r o w n > 0Y 7/4 burrowed clay. 0Y 8/4 Flora: etioulofenestra sp.^ Disσoaster barbadiensis, D. binodosus, D. sublodoensis, D. wemmelensis, Nannotetrina evi.sta.ta, oceolithus eopetagiσus, hiasmolithus eograndis,. californieus, Ericsonia ovalis, E. aitevnans, Sphenolithus sp. Triquetrorhabdulus inversus Flora similar to above Forams G senni, Nuttallides truempyi, lábamina dissonata, Oridorsalis ecuadorensisj Bulimina grata Flora similar to above Zeolitized radiolarians very rare few contaminants from. virginis zone above. Foram fauna as above Flora similar to above Zeolitized radiolarians very rare. F 0Y 6/3 = Y 5/3 Firm burrowed clay in JOY6/3 alternating shades of brown. _/ 5Y 0Y 5/3 7.5Y 0Y 5/3 Foram fauna as above Flora similar to above, plus hiasmolithus aalatus Flora similar to above Very wet brown clay uttings of pale brown and blue gray clay. cc Very rare contaminants from the alooyaletta virginis zone above. Flora similar to above Foram fauna as above 837

86 SHIPBOD SIENTIFI PTY HOLE 9 OE 22 SEDIMENT DENSITY! gm cm i r OMPESSIONL WVE VELOITY km sec' PENETO METE lö~ 2 cm T00 0 WTE ONTENT (wt.) POOSITY (vol.) t % GIN SIZE a0 3 % by wt. % by wt LY SILT SND NTUL GMM DITION t I0 counts/7.6 cm/75 sec t djusted data, see hapter 2 I I I I HOLE 9 OE 23 SEDIMENT DENSITYt gm cm S "i r OMPESSIONL WVE VELOITY km sec ' 2.0 PENETO METE i er 2 cm P00 0 T r WTE ONTENT (wt.) POOSITY (vol.) t % i i r GIN SIZE ao3 % by w«. % by LY SILT SND wt. NTUL GMM DITION t I0 3 counts/7.6 cm/75 sec djusted data, see hapter 2 838

87 SITE 9 HOLE OE TO 392 LITHOL. LITHOLOGY DIGNOSTI FOSSILS BIO- STT. TIME STT. O Lu > a. t- o 0 cm of disturbed brown clay Flora: Discoaster lodoensisl D. bax>badiensis D. sublodoensis, Ericsonia sp.(rims) cc N M Dense brown clay with light yellowish brown bands and mottles and dark gray burrows -ray Mineralogy (Bulk) alc. Qtz. Kao!. Mica Mont. Paly. lin. morph No radiolarians No planktonic forams; BF: Nuttallides truempyi, labamina dissonata, ragonia S p. ore atcher: Forams: Globigerina senni, carinina coalingensis, Nutt, truempyi, ib. havanensis cream: Discoaster barbadiensis, D. lodoensis> D. sublodoensis, Narmotetrina eristata, hiasmolithus expansus^ oaoceolithus eopetagicus> Ericsonia. ovalisj Sphenolithus sp., Trique tr orhabdülus inversus grey-brown: Disaoaster lodoensis, D. barbadiensis, D. kuepperi, D. sublodoensis, rims of Ericsonia ovalis are contaminant radiolarians from the alocycletta virginis zone above HOLE TO 40 m OE 23 LITHOL. LITHOLOGY DIGNOSTI FOSSILS BIO- STT. TIME STT. Dense, brown clay with yellowish brown bands and mottles, dark gray burrows Flora: Discoaster lodoensis, D. barbadiensis i D. wermelensis, D. binodosus, D. kuepperi, Ericsonia ovalis Flora similar to above plus Marthasterites tribrachiatus No radiolarians ore atcher: No radiolarians, Flora similar to Sect. -38 No planktonic forams ö is 5: -^ 839

88 SHIPBOD SIENTIFI PTY HOLE 9 OE 24 METES - - SETION DISTUB. LOG SEDIMENT DENSITYt gm cm OMPESSIONL WVE VELOITY km sec PENETO METE I0" 2 cm PIOO 0 WTE ONTENT (wt.) POOSITY (vol.) t I GIN SIZE a c 3 % by wt. % by w LY SILT SND NTUL GMM DITION t I0 3 counts/7.6 cm/75 sec ,0 0 2 '"I d 3 j I 5 7 J" T 8 *~~ 6 : I t djusted data, see hapter 2 840

89 SITE 9 HOLE OE TO 40 LITHOL. LITHOLOGY DIGNOSTI FOSSILS BIO STT. TIME STT. OY 3/3 Dense, dark brown clay, burrowed dark gray with light yellowish brown mottles. oarse fraction consists of a few fish teeth and pyritized worm tubes No coccoliths No radiolarians are benthonic forams No coccoliths No radiolarians. are fish teeth, No coccoliths N N M lternating brown and very pale brown dense clay bands, average 5 cm thick. 0Y 4/3Grayish-green (5G 6/) 0Y 6/4band at cm in and Sect. 3 0Y 8/4 Fauna as above No coccoliths No radiolarians-fish teeth rare to common. No coccoliths Sloppy, disturbed brown clay. cc [are benthonic forams: Geudryina, Dorothia Flora: Discoaster multiradiatus } D. binodosus, D. gemmeus, D. f. faloatus, D. lentiaularus, Eriaaonia ovalis, Faβaiaulithus sp. No radiolarians 84

90 SHIPBOD SIENTIFI PTY HOLE 9 OE 25 METES j i SETION DISTUB. LOG 4 SEDIMENT DENSITY t gm cm OMPESSIONL WVE VELOITY km sec~' PENETO METE I0" 2 cm PI00 0 WTE ONTENT (wt.) POOSITY (vol.) t % GIN SIZE a 3 % by wt. % by LY SILT SND wt NTUL GMM DITION + I0 3 counts/7.6 cm/75 sec < i i t djusted data, see hapter 2 HOLE 9 OE 26 on-j SEDIMENT DENSITY t gm cm OMPESSIONL WVE VELOITY km sec ' PENETO METE I0' 2 cm PI00 0 I TT WTE ONTENT (wt) POOSITY (vol.) f GIN SIZE ao3 % by wt. LY SILT SND NTUL GMM DITION + I0 counts/7.6 cm/75 sec \ t djusted data, see hapter 2 I 842

91 SITE 9 HOLE OE TO 49 LITHOL. LITHOLOGY DIGNOSTI FOSSILS BIO STT. TIME STT. cc N,F N N,F N N F N M N 5Y 5/4 Dense, light olive gray clay with yellowish brown clay at the top and mottled yellow/ brown in places. Greenish gray clay, mottled with light bluish gray. 5GY_4/ 5GYJ5/ 5~GY 4/ lternating layers of greenish 5GY"6/ 9 ra y anc * dark greenish gray cla j>i y 5GY 6/ Silicified limestone layers at in Sec. 2 5GY 4/ x-ray Mineralogy (Bulk) alc. Qtz. Plag. Mica Mont. lin. morph Flora: Disaoaster multiradiatus, D. gemmeus, D. helianthus, D. falaatus, D. lentiaularis, Eriasonia cava, E. subpertusa, hiasmolithus californious, Scapholithus apertus, Toweius eminens, T. araticulus, T. tovae, Fasaiaulithus tympaniformis, F. involutus, F. sahaubi, Semihololithus kerabyi, S. biskayae, Ellipsolithus macellus, E. distiahus, Heliolithus kzeinpelti, Sphenoli thus primus Λ Neoaoaaolithus sp. Zygodisaus pleatopons, Braavudosphaera discula and reworked retaceous coccoliths Disaoaster multiradiatus, D. helianthus, D. falaatus, Eriasonia aava Flora similar to above (Sect. ) Foram fauna: are planktonics: G. subbotinae, G. aequa, G. pasionensis, aar. coalingensis Flora similar to above Flora similar to above Zeolitized radiolarians common. ore atcher: Zeolitized radiolarians common. Flora similar to above HOLE 9 49 TO 428 OE 26 LITHOL. LITHOLOGY DIGNOSTI FOSSILS BIO- STT. TIME STT. L-J N N M 5GY 4/ 5Y 6/ lternating bands of gray, --5GY 4/ greenish gray and white dense ~5GY ^ Siliifid Silicified limestone l i t bands at 5-6 and Y 4/ -T5~Y~8/ 5GY 4/ 5Y 6/ 5Y 6/2 Dense, uniform,gray pale olive and white clay. No radiolarians. Flora: Disaoaster multiradiatus, D. nobitis, D. gemmeus, D. lentioularis, D. falaatus, Toweius eminens, T. tovae, T. aratiaulus, Sphenolithus primus, Fasaioulithus involutus, F. tympaniformis, Semihololithus kerabyi, S. biskayae, Ellipsolithus maoellus, E. distiahus, Disaolithina plana, Zygodisaus sigmoides, Z. adamas, Z. pleatopons, Saapholithus apertus, Neoaoaoolithus protenus, N. aonainnus, N. junatus, hiasmolithus daniaus,. aff. gigas, Eriasonia aava + reworked retaceous coccoliths 5Y 6/ ~"5Y 8/ 5Y 6/ -ray Mineralogy (Bulk) alc. Qtz. Plag. Mica hi. Mont. lin. morph Flora similar to above Zeolitized radiolarians very abundant. Silicified and corroded Paleocene radiolarians include Lithocampium sp. Phormoayrtis striata One contaminant L. bipes from. virginis zone. Flora similar to above are planktonic forams ore atcher: Zeolitized, silicified and corroded radiolarians abundant. Lithoaampivm sp. abundant, Phormoayrtis striata. Flora similar to above. No forams. 843

92 SHIPBOD SIENTIFI PTY HOLE 9 OE 27 SEDIMENT DENSITYt gm cm OMPESSIONL WVE VELOITY km sec ' 2.0 PENETO METE lö~ 2 cm P00 0 T I WTE ONTENT (wt.) POOSITY (vol.) f % GIN SIZE % by wt % by LY SILT SND wt "49 NTUL GMM DITION t I0 3 counts/7.6 cm/75 sec J I I I I 'djusted data, we hapter 2 844

93 : SITE 9 HOLE OE TO 433m METES SETION LITHOL. SMPLES LITHOLOGY DIGNOSTI FOSSILS BIO- STT. TIME STT. _ cc : -z~ M N,F c M N F ^ u > O LO >- lternating bands of uniform hard gray clay -ray Mineralogy (Bulk) alc. 5.3 Dolo. 6.5 Qtz. 8. Plag. 4.9 Mica 27.3 Mont. 2.0 morph. 5.9 Silicified and corroded radiolarians rare. Zeolitized radiolarians very rare. Lithooampium sp., Bekoma bidarfensis, Phormooyrtis stviata Flora: Disaoaster multiradiatus_, D. nobilis D. germeusj D. lenti cularisj D. falcatus, Toweius eminens, T. tovae 3 T. araticulusj Sphenolithus primus, Pasaiaulith us invotutus t F. tympaniformis; Semihololithus kerabyi> S. biskayae, Ellipsolithus maoellus E. disttchusj Disaolithina plana^ Zygodisous sigmoides, Z. adamas Z. pleotoponsj Soapholithus apertus, oinnus, N. Qunotus, hiasmolithus daniousferiosonia oava 3 plus reworked retaceous coccoliths No coccoliths No forams Silicified and corroded radiolarians very rare. Lithooampiwn sp., (?) P. striata 3 i-i!n -t-i <a to o to LU LU O _l <c LU ore atcher: Zeolitized radiolarians very abundant. Silicified and corroded radiolarians very rare-lithooampium sp.. Flora similar to above Forams: Globigerina velascoensis> oarinina esnaensis 845

94 SHIPBOD SIENTIFI PTY HOLE 9 OE 28 SEDIMENT DENSITY t gm cm OMPESSIONL WVE VELOITY km sec PENETO METE I0* 2 cm P00 0 I I >< WTE ONTENT (wt POOSITY (vol.) f % I I I I GIN SIZE % by wt. LY SILT SND ao % by wt. NTUL GMM DITION t I0 counts/7.6 cm/75 sec J> tdjusted data, see hapter 2 J I I I I I 846

95 SITE 9 HOLE ]9 443 TO 452 m OE 28 LITHOL. LITHOLOGY DIGNOSTI FOSSILS BIO- STT. TIME STT. N8 2 cc y... :.v.r : M N, F NF~ 5GY_6/ J5YJ/ 5Y_8/ 5Y_ 4/ 5Y 6/ 5Y 7/ Beds of uniform clay in various shades of gray. alcareous burrows at Very hard sandstone layers at in Section 2. Mineralogy (Bulk) not calculated Flora: D. nobilis, Disaoaster multiradiatus Λ D. gemmeus, D. cf. faleatus, Sphenolithus primus, Fasoiσulithus involutus, F. tympaniformis } Towei us oratiautus, T. tovae, T. eminens, hiasmolithus bidens,. danicus,. eograndis, Eriasonia aava, Semihololithus biskayae } S. kerábyi, Hel iolithus kleinpell ij Ellipsolithus distichus, E. macellus, Zygodiseus plectopons, Beoaoaoolithus sp. Flora similar to above Zeolitized radiolarians common. few silicified spumellarians. Forams: hiloguembelinids, rare planktonics ore atcher: Zeolitized radiolarians common. orroded and silicified radiolarians common (20-30 species): Lithocampiwn sp., Bekoma bidarfensis, Phormocyrtis striata, Stioh.omi.tra (?) sp. Flora similar to above, less Disaoaster multiradiatus Barren of forams ore atcher 847

96 SHIPBOD SIENTIFI PTY HOLE 9 OE 29 SEDIMENT DENSITYt gm cm OMPESSIONL WVE VELOITY km sec"' PENETO METE I0" 2 cm WTE ONTENT (wt.) POOSITY (vol.) t PIOO T \ I I I I % GIN SIZE % by wt. LY SILT SND ao %by wt. NTUL GMM DITION t I0 3 counts/7.6 cm/75 sec I I I I I I + djusted data, see hapter 2 848

97 SITE 9 HOLE TO 465 m OE 29 LITHOL. LITHOLOGY DIGNOSTI FOSSILS BIO- STT. TIME STT. 2 N,F M N Light gray silty clay; hard, laminated, slightly burrowed Dark gray indurated clay ross bedded calcareous, sandstone. Light gray uniform clay Flora; pisσoaster germeus, D. nobilis, Fasoiaulithus tympaniformis, F. involutus Semihololithus kerabyi, S. biskayae, Sphenolithus primus, Toweius cvatiaulus, T. eminenβj Ellipsolithus distichus,. maoetius, üeliolithus kleinpelli, H. cf. viedeli, Disoolithina plana, Eriasonia aava, hiasmolithus bidensj. aff. gigas, ruciplaeolithus inseadus, Saapholithus apertus, Neocoaaolithus sp., plus reworked retaceous coccoliths Indeterminable forams Flora similar to above, less Semihololithus biskayae, S. kerabyi Fauna essentially barren Flora similar to Sect Silty clay alcareous sandstone Indurated light gray clay Flora similar to Sect Slightly burrowed green gray clay Dense gray silty clay Flora similar to Sect Y 6/ alcareous sandstone Indurated green-gray clay -ray Mineralogy (Bulk) alc. Qtz. Plag. Mica Mont. lin morph ore atcher: Silicified radiolarians rare. Lithocampium sp. Flora similar to Sect Forams: G. aauta-velasooensis gp plus Boiivina, Melonis, discorbids, chiloguembelinids 849

98 SHIPBOD SIENTIFI PTY HOLE 9 OE 30 SEDIMENT DENSITYt gm cm OMPESSIONL WVE VELOITY km sec" PENETO METE I0" 2 cm WTE ONTENT (wt.) POOSITY (vol.) t % P00 I T I I I I I GIN SIZE ao3 % by wt. % by LY SILT SND NTUL GMM DITION t I0 counts/7.6 cm/75 sec J I I I! I I I t djusted data, see hapter 2 850

99 SITE 9 HOLE l]9 OE TO 502 m V5 LITHOL. LITHOLOGY DIGNOSTI FOSSILS BIO- STT. TIME STT. EMPTY Whole core consists of short sections of solid rock. M N7 N8 N7_ N8 5Y 6/ Whole core is indurated dense clay. Dip ^0 at bottom of Section Burrowed at 0-37 and in Section 2 Flora: Disaoaster gemmeus, D. nobilis, Fasaiaulithus tympaniformis, F. involutusj Sphenolithus primus, S. anarthopus, hiasmolithus daniaus, Toweius eminens> T. oratiaulus, T. tovae, Ellipsolithus maaellus, E. distiahus, Eriasonia aava, Thoraaosphaera sp. Neoaoaaolithus sp. Braarudosphaera imbriaata, B. bigelowi, plus reworked retaceous coccoliths Flora similar to above 5Y 4/ 5Y 6/ Dark olive gray laminations at 0-0 and in Section 3 laminations dip at ^0 -ray Mineralogy (Bulk) alc. Qtz. Mica Mont. lin. morph M N *N3_ N3 and 5GY 6/ ü_ 5Y 6/ 5Y 7/ Dark gray laminations at and around 75 in Section 5 Small faults cut laminations? compaction Flora similar to above, less Disaoaster nobilis Flora similar to Sect. 4 5GY 8/ cc 5Y 6/ Some laminae in Section 6 dip at ^5. Flora similar to Sect. 4 Forams: hiloguembelinids and small globigerinids Zeolitized radio!arians common. Silicified and corroded radio- arians rare: Lithoaampium sp., (?) istiahomitra alamedaensis Flora similar to Sect. 4 Forams rare; Globorotalia velasaoensis 85

100 SHIPBOD SIENTIFI PTY HOLE ] 9 OE 3 SEDIMENT DENSITY t gm cm OMPESSIONL WVE VELOITY km sec~ PENETO METE T PIOO 0 cm I WTE ONTENT (wt.) POOSITY (vol.) t % i i r GIN SIZE a 3 % by wt. % by LY SILT SND wt NTUL GMM DITION t I0 3 counls/7.6 cm/75 sec \ J I i i i i t djusted data, see hapter 2 852

101 SITE 9 HOLE OE TO 552 m LITHOL. LITHOLOGY DIGNOSTI FOSSILS BIO STT. TIME STT. EMPTY 5GY 6/ 5Y 5/ N4 5GY 6/ 5GY 6/ Whole core consists of several pieces of solid rock. ll dense, indurated gray clay. Laminae dip ^0 Flora: Heliolithus kleinpelli, H. cf. riedeli, Fasoioulithus tympaniformis, F. involutus 3 Toweius tovae, T. eminens, T. craticulus, Ellipsolithus distichus, E. maoellus, Sphenolithus primus, S. anarr>hopus } Soapholithus apertus, Braarudosphaera bigelowi, B. disoula, ruoiplaoolithus tenuis, hiasmolithus danicusy. bidens,. aff. gigas, Zygodisβus pleatopons, Eriasonia eava, E. subpertusa, Thoraaosphaera sp. Neocoooolithus sp. plus reworked retaceous coccoliths Laminae of dark gray immediately below dark gray layer Flora similar to above, less Zygodisous pleatopons N7 White mottles 5G 8/ Laminae dip ^ 5G~8/ W n i t e mottles 5Y 5/ -ray Mineralogy (Bulk) M 5Y 6/ 5GY 7/ alc. Qtz. Plag. Mica Mont. lin. morph Flora similar to Sect. 2 5Y 6/ Flora similar to Sect. 2 5GY 6/ Laminae dip Flora similar to Sect. 2 cc 5G 7/ ore atcher: Very n are si icified radiolarians, Flora similar to Sect. 2 Fauna: Barren 853

102 SHIPBOD SIENTIFI PTY HOLE 9 OE 32 SEDIMENT DENSITY t gin cπf OMPESSIONL WVE VELOITY km sec" PENETO METE I0' 2 cm PI00 0 I I WTE ONTENT (wt. POOSITY (vol.) f % I I I I GIN SIZE ao. % by wt. % b LY SILT SND w t NTUL GMM DITION t 0 counts/7.6 cm/75 sec J j 47 J I I I I I t djusted data, see hapter 2 854

103 SITE 9 HOLE OE TO 594 METES i SETION j LITHOL. SMPLES LITHOLOGY DIGNOSTI FOSSILS BIO- STT. TIME STT. I I EMPTY m 2 mi N N N F Whole core is short sections of solid rock. 5Y 6/ ~ _ Dense indurated gray clay. 5Y 5G 5Y 5Y 5/ Intense burrowing at 5-8 and in Section 2. ~8/l Laminae dip at M0 5/ Flora: Heliolithus kleinpelli, H. cf. riedeli, Fasaioulithus involutus, F. tympaniformis, Toweius araticulus, T. tovae, T. eminens, ruoiplaaolithus tenuis, hiasmolithus daniaus,. bidens, Eriasonia aava, E. subpertusa, Sphenolithus primus, S. anarrhopus, Zygodisaus sigmoides, Z. cf. pleotopons, Ellipsolithus maaellus, E. distichus, Thoraaosphaera sp., Neocoσcolithus sp., yclolithusl robustus, plus reworked retaceous coccoliths Flora similar to above, plus Braarudosphaera bigelowi, B. imbriβara, Miorantholithus arenulatus, Markalius inversus ore atcher: No radiolarians. Flora similar to Sect. 2. Forams: Globigerina triloculinoides, G. triangularis Heliolithus kleinpelli LTE PLEOENE 855

104 SHIPBOD SIENTIFI PTY HOLE 9 OE 33 SEDIMENT DENSITY! gm cm OMPESSIONL WVE VELOITY km sec" PENETO METE 0T 2 cm P00 0 I T WTE ONTENT (wt.) POOSITY (vol.) t % GIN SIZE % by wt. LY SILT SND ao, NTUL GMM DITION t I0 3 counts/7.6 cm/75 sec \ I j I i i + djusted data, see hapter 2 856

105 SITE 9 HOLE 9 OE TO 600 r LITHOL. LITHOLOGY DIGNOSTI FOSSILS BIO- STT. TIME STT. J. _ GP N8 5GY 6/ N7 5GY 6/ 5Y 5/ 5Y_6/ Whole core is several short sections of solid rock Dense indurated gray clay and caicarenite alcarenite has convolute bedding and lamination Flora: Fasciaulithus tympaniformis, Toweius eminens, T. tovae, T. βraticulus, Ellipsolithus distiahus 3 E. macellus, Eriósonia cava, E. subpex>tusa, yelolithus vohustus, hiasmolithus sp, ruaiplacolithus tenuis, Zygodisous sigmoides, Sphenolithus primus, S. anarrhopusj Thoraoosphaera sp., Neoaoacolithus sp., N. junatus plus reworked retaceous coccoliths 5Y 5/ 56/ 5Y 5/ Flora similar to above, poorer 5Y 6/ 5Y~4/ 5Y~6/ Slickensides at in Section 2 Flora similar to above, less Toweius eminens, T. tovae ~~ White "mottling" at in Section 3 5Y 5/ ore atcher: No radiolarians Flora similar to above, less Toweius nensy T. tovae Fauna: Barren 857

106 SHIPBOD SIENTIFI PTY HOLE 9 OE 34 (/) aü w w Σ - z o TI O βá Q SEDIMENT DENSITYt gm cm OMPESSIONL WVE VELOITY km sec PENETO METE I0" 2 cm PI00 0 I WTE ONTENT (wt.) POOSITY (vol ) t % I I I GIN SIZE ao3 7c by wt. % by LY SILT SND NTUL GMM DITION t 0 counts/7.6 cm/75 sec i 4 t djusted data, see hapter 2 I I I 858

107 SITE 9 HOLE OE T0 630 m METES SETION ~j LITHOL. SMPLES LITHOLOGY DIGNOSTI FOSSILS BlOr STT. TIME STT. I I I M N F N Greenish gray, very hard, fine grained marly clay. 5GY 6 /' Indurated Burrowed horizons have sharp top and transitional lower 5G7 4/ P art Pyritized burrow at 45 Dip ^20 -ray Mineralogy (Bulk) alc Qtz. 4.0 Mica 3.6 Mont. 2.9 ris. 8.8 morph Flora: Eriosonia aava ore atcher: Fauna: Barren Flora: Fasaiaütithus tympaniformis 3 Markalius inversus, Braarudosphaera bigelσwi, Prinsius bisulous, ruai~ plaaolithus tenuis, hiasmolithus danious, yclotithus robustus, Eriosonia oava, Ellipsolithus distiahus Soapholithus apertus, Sphenolithus primus s S. anca>rhopus, Neoaoaaolithus sp. iv. junotusj Thoracosphaera sp. plus reworked retaceous coccoliths orroded and silicified radiolarians rare. Fasoiaulithus tynrpaniformis LTE PLEOENE 859

108 SHIPBOD SIENTIFI PTY HOLE 9 OE 35 SEDIMENT DENSITY! gm cm OMPESSIONL WVE VELOITY km sec ' PENETO METE I0" 2 cm WTE ONTENT (wt.) POOSITY (vol.) f PIOO T I I I I I % GIN SIZE a 3 % by wt. % by LY SILT SND wt NTUL GMM DITION t I0 3 counts/7.6 cm/75 sec J \ + djusted data, see hapter 2 860

109 SITE 9 HOLE OE T0 648 m LITHOL. LITHOLOGY DIGNOSTI FOSSILS BIO STT. TIME STT. 5GY 5/ This core is in several short sections of solid rock, ompact, indurated laminated clay Flora: Fasoiculithus tympaniformis, F. úlii, F. janii, Sphenolithus primus, S. anarrhopus, Toweius cf. oratiaulus, El~Lipsolithus distiahus, E. macellus, ruaiplaoolithus tennis,. inseaduε, yalolithus robustus, Zygodisaus sigmoides, Neoaooaolith.es sp., N. junctus plus reworked retaceous coccoliths 5GY 4/ Burrowed, dark olive clay. N M 5Y5/ Indurated gray clay Flora similar to above, plus Braarudosphaera bigelowi, B. disoula, B. imbriaata Dense indurated claystone N M M 5Y 4/ 5Y "6/2 5Y 6/ Dark Light gray clay olive clay Slightly mottled dense indurated claystone Flora similar to Sect. 2, plus Fasoioulithus biztii 5Y 5/ cc M N M 5Y_5/ 5Y~7/2 5YJ5/ 5Y 7/ 5Y 5/ 5Y 7/2 Green/gray laminated claystone Dense, indurated uniform, fine grained claystone -ray Mineralogy (Bulk) alc Qtz. 4.6 Mica 3.3 ris morph Flora similar to above plus Fasoiaulithus ore atcher: Zeolitized radiolarians common: Stiβhomitra sp. orroded and silicified radiolarians rare: Lithoaampium sp.. Flora similar to above, plus Prinsius rnartinii, Eriasonia aava, Fasoiaulithus billii Fauna: Barren 86

110 SHIPBOD SIENTIFI PTY HOLE 9 OE 36 is on-j SEDIMENT DENSITY t gm cm OMPESSIONL WVE VELOITY km see ' PENETO METE lt 2 cm PI0O I0 WTE ONTENT (wt.) POOSITY (vol ) t I I I GIN SIZE a0 3 % by wt. % by LY SILT SND WI NTUL GMM DITION + 0'' counts/7.6 cm/75 sec djusted data, see hapter 2 I I I 862

111 SITE 9 HOLE 9 OE TO 662 m 3 METEI 2 SETI< LITHOL. SMPL 3 LITHOLOGY DIGNOSTI FOSSILS BIO- STT. TIME STT. I I I EMPTY - - _ 2 _ 2 Ill III III III : i l l I I I I I I I I I I I I! I! I! I! I I I I I I I I I! I! I N N 5Y 5/ 5Y 4/ _5Y_ 4/ 5Y 6/ 5Y 4/ Dense, lithified claystone with loadcasts, etc. Hard dark gray claystone Lithified claystone with black burrows Fasoiouli~bhus tunpaniforvnis F. billü. F. ulii, F. janii, Sphenolithus primus, Toweius oratiaulusy Ellipsolithus maaellus, Eriasonia aava, E. robusta, Braarudosphaera bigelowi, hiasmolithus daniousy ruaiplaoolithus tenuis, Neoaoaaolithes sp. Thoraaosphaera sp. plus reworked retaceous coccoliths Flora poorer than above Flora poorer than above I'!'!! i i i' i i! 5G 8/ B urrowec l P3le green O hi I I hi I I Iiii I I I I I I I I I I I I i l i l i l i 5Y 4/ passing into S Si -M OENE - " ^ /. Λ V 5 Y 5/ Hard ir durated gray clay Sandstone ithu PLE 5 _ - 4 LU 'IMM I 'IMM I IMM ill' "jr^-7- N N F 5G 8/ Gray green burrowed clay 5G 8/ Slightly burrowed gray green clay 5Y 5/ passing into Uniform gray clay getting siltier towards base Flora poorer than above ore atcher: isilicified and corroded radiolarians common: Lithoaampium sp., Bekoma bidavfensis, Phormooyrtis striata, mphipyndax stoaki are, well preserved contaminant Middle Eocene species from the Theocampe mongolfieri zone (25-30 species). Flora similar to above, plus Braarudosphaera discula, Zygodisaus sigmoides Fauna: Barren Fascia 863

112 SHIPBOD SIENTIFI PTY HOLE 9 OE 37 SEDIMENT DENSITYt gm cm I I OMPESSIONL WVE VELOITY km sec PENETO METE I0" 2 cm P00 I0 WTE ONTENT (wt.) POOSITY (vol ) t % I I I I GIN SIZE ao3 % by LY SILT SND w( NTUL GMM DITION t I0 3 counts/7.6 cm/75 sec J J J J J j I I I I I I I t djusted data, see hapter 2 864

113 SITE 9 HOLE 9 OE TO 674m LITHOL. LITHOLOGY DIGNOSTI FOSSILS BIO STT. TIME STT. GP 5Y 5/ Uniform lithified gray claystone 5Y 5/ Gray lithified claystone with load casts and other primary structures Slickensides dipping at ^25' Flora: Eriosonia oava, Fasaiaulithus tympani form-is j F. ulii, F. billii, F. Qanii, Sphenolithus primus, Toweius aratiaulus, Prinsius martinii, P. bisulcusj yololithus robustus, Braarudosphaera discula, B. bigelowi, B. imbricata, Markalius inversus 3 rueiplaaolithus tenuis,hiasmolithus danious,. bidens, Zygodisaus sigmoides, Ellipsolithus maaellus, NeoooQcolith.es sp. plus reworked retaceous coccoliths Flora similar to above 5Y 4/ 5Y 5/ Slickensides along entire length Gray lithified claystone Flora similar to above 5Y~4/ Slickensides at _Y 6/ Gray sandy claystone M 5Y 4/ Dark gray indurated clay Flora similar to above cc 5Y 7/ Greenish gray claystone dipping ^25 -ray Mineralogy (Bulk) alc. Dolo. Qtz. Plag. Mica Mont. morph Flora similar to above ore atcher: No radiolarians Flora similar to above Fauna: Barren 865

114 SHIPBOD SIENTIFI PTY HOLE 9 OE 38 SEDIMENT DENSITYt gm cm OMPESSIONL WVE VELOITY km sec ' PENETO METE I0" 2 cm WTE ONTENT (wt > POOSITY (vol.) t PI i r i i r T % GIN SIZE % by wt. LY SILT SND ao3 % b> NTUL GMM DITION t 0' counts/7.6 cm/75 sec j i i t djusted data, see hapter 2 866

115 SITE 9 HOLE 9 OE TO 686 m LITHOL. LITHOLOGY DIGNOSTI FOSSILS BIO- STT. TIME STT. 5Y6/ Gray indurated clays tone -ray Mineralogy (Bulk) 5Y 6/ alc. Qtz. K-Feld Plag. Mica morph Dense lithified claystone Flora: Fasaiculithus tympaniformis, F. ulii Sphenolithus primus, Toweius oratioulus, Braarudosphaera bigelowi, Eriasonia oava, yelolithus robustus plus reworked retaceous coccoliths ~ßl 5/ 5Y 8/ Gray burrowed claystone Flora similar to above plus Ellipsolithus maoellus, E. distiohus Flora similar to above Flora similar to above N.M N 2.5Y5/4Laminated red/brown claystone 2J5Y 3/4 2.5Y 5/4 5Y 5/ ed brown claystone lternating layers of redbrown and gray clay. ed layer: are mottled, gray layers have sedimentary structures Flora similar to above Flora similar to above, no Fascioulithus plus Ellipsolithus maoellus, E. distiohus Forams: Globigerina trilooulinoides, chiloguembelinids Flora similar to Sect. 3-6 \Λ cc M Mineralogy (Bulk) alc Dolo..3 Qtz. 4.7 Mica 6.9 Mont. 4.6 morph ore atcher: No radiolarians. Flora similar to Sect. 3-6 Forams: G. pseudobultoides, G.varianta, G. angulata, G. ooniootrunoata, G. ekrenbergij G. triloaulinoides 867

116 SHIPBOD SIENTIFI PTY HOLE 9 OE 39 SEDIMENT DENSITYt gm cm OMPESSIONL WVE VELOITY km sec" PENETO METE 0T 2 cm PIOO io T I i WTE ONTENT (wt.) POOSITY (vol.) t GIN SIZE % by wt. % by LY SILT SND *' ao 3 NTUL GMM DITION t I0 3 counts/7.6 cm/75 sec T j I I I I I I I + djusted data, see hapter 2 868

117 SITE 9 HOLE TO 699 OE 39 METES SETION 2 LITHOL. SMPLES N N M N,F LITHOLOGY Light gray and white lithified claystone N7 Dip -v. 20 Mottling -ray Mineralogy (Bulk) N9 alc Qtz..4 morph N7 DIGNOSTI FOSSILS Flora: Toweius cvatioulus, Ellipsolithus distichus, Zygodisβus sigmoides > Markalius invevsus, Braarudosphaera bigelowi, B. disaula, B. imbvicata, Prinsius bisulaus^ Miarantolithus sp. hiasmolithus danious, ruaiplaoolithus tenuisj Eriasonia aava, yalolithus cf. robustus, Neoeoacolithes sp. plus reworked retaceous coccoliths Flora similar to above Flora similar to above Fauna: Barren BIO STT. STT. _ UD c.. Gray and red-brown 2.5Y5/4 claystone _ üv y \..." ^r: - ^ " ^ ^ _S N M N N7 -- N6 --~N6 2.5Y 5/4 N7 N8 lternating gray and red brown clays tone Mottling Gray indurated clay., moderately mottled Flora similar to above Flora similar to above c- lus ithus mac.lipsol Eq LTE F LEOENE 7 S cc ~JZ JL Jr" T Λ^_ \ ~ ^~ «- NI M N -ray Mineralogy (Bulk) alc N7 Dolo..8 Qtz. 3.3 Mica 9. morph N8 Flora similar to above ore atcher: Two silicified radiolarians Flora similar to above Forams hiloguembelinids, G. triloculinoides, G. pseudobulloides, Keeled globorotaliids {langulata) i l/\ O a. 869

118 SHIPBOD SIENTIFI PTY HOLE 9 OE 40 SEDIMENT DENSITY t gm cm.0 l.s OMPESSIONL WVE VELOITY km sec ' PENETO METE 0" : cm PI00 0 I I WTE ONTENT (wt.) POOSITY (vol.) t % GIN SIZE ao, % by wt. % by LY SILT SND wt NTUL GMM DITION t 0'' counts/7.6 cm/75 sec I I I I I I t djusted data, see hapter 2 870

119 SITE 9 HOLE TO 7m OE 40 LITHOL. LITHOLOGY DIGNOSTI FOSSILS BIO- STT. TIME STT. Light gray lithified clay, uniform at the top but many load casts and slump structures towards the bottom of Section Sandy indurated claystone Flora: Ellipsolithus macellus, Eriσsonia aava, Zygodiscus sigmoides, yclolithus robustus, Prinsius max>tinii, Braarudosphaera bigelowi, Miorantolithus sp., ruciplacolithus tennis, Neoeoccolith.es sp. plus reworked retaceous coccoliths Flora similar to above Flora similar to above Light gray indurated claystone with several widely spaced laminae dipping at ^5 Flora similar to above Flora similar to above, less Ellipsolithus macellus Flora similar to above, less Ellipsolithus macellus ore atcher: Flora similar to above, plus hiasmolithus danicus, less Ellipsolithus macellus No radiolarians 87

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