9. SITE 209
The Shipboard Scientific Party1
With Additional Contributions From
Derek Burns, New Zealand Oceanographic Institute, Wellington, New Zealand

Location: Queensland Plateau
Position: 15°56.19'S, 152°11.27'E
Water Depth: 1428 meters
Total Penetration: 344 meters

Contour interval 400 fathoms. (After Mammerickx, Chase,
Smith, and Taylor, 1971. Bathymetry of the South Pacific,
Charts 11 and 12: Scripps Institution of Oceanography,
California.)
Summary: Foraminiferal ooze and nannofossil ooze overlie the regional unconformity (late Oligocene/late Eocene) below
which is sand-bearing foraminiferal ooze and chert. The prominent regional acoustic reflector has been identified as a late
Eocene chert horizon. Terrigenous detrital sands and silts are a prominent component of the middle Eocene
glauconite-bearing calcareous silty sandstone to sandy siltstone in which the hole was terminated.

BACKGROUND AND OBJECTIVESGeneralSite 209 was proposed to examine the age and structural
history of the Queensland Plateau, the relationship of theplateau to the adjoining Coral Sea Basin, and to provide abiostratigraphic sequence from this subequatorial portionof the region traversed by Leg 21.
Prior to site survey, several seismic profiles had been run
over the plateau, and the regional continuity of the1

Robert E. Burns, NOAA-Pacific Oceanographic Laboratories,
University of Washington, Seattle, Washington, Co-Chief Scientist;
James E. Andrews, University of Hawaii, Honolulu, Hawaii),
Co-Chief Scientist; Gerrit J. van der Lingen, New Zealand Geological
Survey, Christchurch, New Zealand; Michael Churkin, Jr., U. S.
Geological Survey, Menlo Park, California; Jon S. Galehouse, San
Francisco State College, San Francisco, California; Gordon H.
Packham, University of Sydney, Sydney, New South Wales,
Australia; Thomas A. Davies, Scripps Institution of Oceanography,
La Jolla, California; James P. Kennett, University of Rhode Island,
Kingston, Rhode Island; Paulian Dumitrica, Geological Institute of
Romania, Bucharest, Romania; Anthony R. Edwards, New ZealandGeological Survey, Lower Hutt, New Zealand; Richard P. Von
Herzen, Woods Hole Oceanographic Institution, Woods Hole,
Massachusetts.

prominent acoustic reflector had been established. Sitesurvey was conducted by R/V Kona Keoki, and data fromthe survey were the principal sources of information for
selecting the specific drilling site.
Review of the proposed site by the JOIDES Panel on
Pollution Prevention and Safety indicated that the site andthe drilling program were satisfactory with continuous
coring, moderate drilling precautions, and standard abandonment procedures.
Site Survey

The site survey for Site 209 was conducted by the R/VRana Keoki in September 1971 and covered a section of
the outer plateau and the slope break (Figure 1). Prior to
the site survey, several seismic, reflection profiles across the
Queensland Plateau (e.g., Ewing et al., 1970) had established the regional continuity of a prominent reflector at an
average of 0.25 sec subbottom. Profiles obtained during thesite survey (Figure 2) show this reflector and several others
giving rise to a regularly layered appearance of the plateau.
Many of these reflectors crop out at the plateau margin (seeFigures 1 and 3), and the depth of the prominent regionalreflector outcrop is an approximately 2000 meters ofwater. The pattern of exposure suggests slumping of blocks

333

SITE 20918'

151°30'E

42

Figure 1. Bathymetry of proposed area of Site 209. Outer margin of the Queensland Plateau. Dashed line marks outcrop of
0.25 sec reflector. Actual site was occupied to the southeast of this area. Kana Keoki site survey September 1971.

with glide planes on several of the horizons. In thenortheast corner of the site survey area is a small reentrant.
This appears to be a slump scar on the 0.25-sec reflector
which may have acted as a submarine canyon whichchanneled shallower debris off the plateau. An indistinct
basement reflector occurs at depths of 0.75 to 1.00 sec
subbottom throughout the surveyed area, rising irregularly
to within 0.35 sec of the sea floor.
OPERATIONS
Site Approach

The drilling site was selected on the Kana Keoki track to
the original site survey at a point at which the acoustic
basement rose to within 0.38 sec subbottom, and the0.25-sec reflector was clearly defined. Site approach (Figure4) was along the Kana Keoki track on a course of 320°T.
The beacon was dropped underway after an initial crossing334

to verify the site structure. The basement reflector becomesmuch deeper south of the site.

Sonobuoy
The Site 209 sonobuoy record (Figure 5) is considerably
more reflective than the underway profiles. Reflectors are
generally strong, and all major ones are picked up at the
low frequency settings (10 to 40 Hz). The acoustic
basement (Reflector 5) and the 0.25-sec reflector (Reflector 4) give the strongest signals. These are broad bands 0.1
to 0.2 sec thick. On the 20 to 160 Hz setting the basement
reflector shows closely spaced signals (whether real orreverberation cannot be determined) to a depth of over 1.0
sec subbottom. The character of these signals suggests thehorizons represent marked changes in acoustic impedance
and that they may well be layer structure s-presumably

Figure 2. Seismic profile from Kana Keoki site survey showing Plateau structure.
lithified sediments. Table I 2 summarizes the sonobuoy dataand initial interpretations.
Drilling Program

The first core (Table 2) was aboard at 1010 on 28
December, and a continuous coring routine was establishedfollowing the recommendations of the Safety and Pollution
Prevention Panel. Recovery was good down to 54 meters
following which practically no recovery was made for theinterval 54 to 119 meters. The sediment in this interval wasa well-sorted foraminiferal ooze which appears to flow as a
fluid when wet. Because of the negligible recovery, analternation of wash and core was run through the interval
119 to 196 meters with very slight improvement inrecovery. At 196 meters the continuous coring routine wasreestablished and was continued to the bottom of the holeat 344 meters.
The string was then retracted to the mud line, and Hole
209A was spudded at 1515 on 29 December. This was totest the new prototype piston corer. The test was unsuccessful and the corer jammed at the bit. The string was
secured and the core (Table 3) returned when the bit wasrecovered.
Two downhole temperature measurements were made inHole 209; the planned attempt at 209A was scratched when
the piston corer jammed.
The site was abandoned at 2200 on 29 December 1971.
Final correlations of sonobuoy profiles using laboratorymeasured velocities, other physical properties, and lithologic
boundaries are presented in Part II of this Initial Report.

LITHOLOGY
GeneralSite 209 was continuously cored to a depth of 344
meters below the sea floor. Thirty-four cores wereattempted, but 11 of these had no core recovery. The
reason for the low core recovery is uncertain but wasprobably due to a very uneven hardness of the sediments
and pumping during the coring process. In addition, theevenly sized foraminiferal ooze that was present in much of
the section was probably disaggregated during coring andran out of the core barrel. In Cores 15, 16, and 20 gradedbedding and sorting of cuttings indicate their suspension
and settling in the drilling fluid.
The lithology in this hole can be conveniently subdivided into three units. From top to bottom they are:1) Unit 1 (0 to 140 m)—foraminiferal ooze and nannofossil ooze (late Oligocene to Pleistocene)2) Unit 2 (140 to 275 m)—sand-bearing foraminiferal
ooze and chert (middle Eocene to late Eocene)3) Unit 3 (275 to 344 m)-sand-rich foraminiferal
limestone with secondary chert filling of voids (middle
Eocene)Unit 1 (Foraminiferal Ooze and Nannofossil Ooze)
This unit, penetrated in Cores 1 through 14, forms theupper part of the sequence. The sediment is composed ofcarbonate with less than 10% insoluble minerals, mostly
silt-sized quartz but also including traces of detrital feldspar
and volcanic glass.

335

SITE 209

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Figure 3. Seismic profile from site survey showing outcropping of'0.25-sec reflector. /?/KKana Keoki.

Most of the carbonate grains are sand- and silt-sized
fossils. Foraminifera and nannofossils are by far the mostabundant, but rare echinoderm, bryozoan, and mollusc
fragments are also present. There is a substantial amount ofangular sand- and silt-sized carbonate grains that partly
represent broken fossils. However, some of the carbonate
grains are euhedral (scalenahedra) and probably represent
authigenic sparry calcite as overgrowths on clastic grains
and fossils and interstitial cement.
Cores 1 and 2 at the top of the hole are very paleorange-grayish orange, while Cores 3 through 5 are white.
This color change approximates the Pliocene-Pleistocene
boundary.
The part of Unit 1 that lies below Core 6 (the interval
55-145 meters below the sea floor) is composed almost
entirely of foraminifera. Nannoplankton form only about
5% of the ooze. The resulting sand-sized sediment is wellsorted and may reflect current action that has winnowedout most of the smaller silt-sized nannoplankton. The
presence of a few apparently reworked benthonic foraminifera in the predominantly planktonic foraminifera ooze
may also reflect transport to the site by bottom currents.
Delicate spines preserved on many of the planktonic
foraminifera, however, indicate no major bottom transport
within the site area. The contact with Unit 2, although notrecovered in the cores, appears to be an abrupt lithologicchange and seems to correlate with a break in the336biostratigraphic record spanning the early and middle
Oligocene.
Unit 2 (Sand-bearing Foraminiferal Ooze and Chert)
The samples recovered from this unit (Cores 15 through27) are believed to represent thin layers of silicified
limestone and chert within a generally unlithified section offoraminiferal ooze. In contrast to the overlying essentiallypure carbonate sequence, Unit 2 has about 10% to 30%
detrital silt and very fine sand grains. Most of these arequartz and feldspar, but both light and dark volcanic glass
and amphibole are present. In addition, there are a few
grains of bright green glauconite. Routine X-ray analyses
indicate substantial quantities of cristobalite, tridymite, andclinoptilolite in the lower part of this unit. Some of thecristobalite may be a product of biogenous opal reacting toform secondary chert. Because of pumping during drilling,
it is hard to know which sections are most representative of
the softer parts of the unit. Cores 23 through 25 and 27
have homogeneous foraminiferal ooze intervals that seem tobe least disturbed and mixed by drilling.
The hard layers are silicified limestone (porcellanite)
replaced irregularly by darker (olive gray) chert. Texturaldetails in thin section suggest every step in the process ofchert replacement of foraminiferal ooze may be present.
The original bioclastic texture is preserved to some degree
in all of the chert. A biogenic origin for the chert is likely as

SITE 209

9

ji
fi

Figure 4. Seismic profile along approach to Site 209. Glomar Challenger December 1971.
there are abundant siliceous sponge spicules in Cores 23 and24 of the unit.
Unit 3 (Sand Foraminiferal Limestone with Secondary
Chert Filling of Voids)
The contact between Units 2 and 3 seems to be
gradational with a downward increase in detrital silt andsand from Core 27. Unit 3 is composed of more than 50%
noncarbonate material, mainly secondary chert (including
colloform opal, microcrystalline quartz, cristobalite, andtridymite) but including up to 15% very fine grained sandand silt. Like the overlying unit, the carbonate fraction iscomposed of foraminifera, nannofossils, broken shelly
fossils, and microcrystalline and sparry calcite cement. Mostof the detrital sand grains are quartz and feldspar. Most ofthese grains are subangular, and some of the grains have
impurities suggesting a terrigenous, rather than subaerial
explosive volcanic origin.
Grains of glauconite, hornblende, dark and light volcanic
glass, devitrified glass, together with argillaceous material,
give the rock a graying olive to dusky yellow green colorthat is darker than that of the overlying more calcareous
unit.

337

SITE 209
TABLE 1Site 209 Sonobuoy Data

SITE 209>

Reflector

Depth
(sec)

1

0.08

2

0.12

3

0.21

4

0.25

5

0.31

6

0.38

NatureStrong, good low
frequency
Strong, good low
frequency
Strong, good low
frequency
Very strong, good
low frequency,
regional reflector
Moderate, no low
frequency
Very strong, good
low frequency,
acoustic basement

Estimated
Velocity
Structure(m/sec)Estimated
Depth
(m)

1500

60

1500

90

1500

157

2500

207

2500

282

4000

422

Sequence of Geologic events Interpreted from Lithology
Late Middle Eocene
Deposition in relatively shallow water (probably on thecontinental margin) of bioclastic (sediment) rich in foraminifera and containing subordinate terrigenous silt and sand.
The presence of glauconite grains with authigenic
mammillary-shaped surfaces indicates a marine origin inwater depths less than 100 fathoms (Williams, Turner, andGilbert, 1954). The fresh glass suggests volcanic ash showers
from volcanoes of intermediate composition. On the other
hand, some of the more altered volcanic detritus androunded quartz may have come from land.

Latest Middle Eocene through Late Eocene
Gradual deepening of the site of deposition and reduction of terrigenous detritus reaching the site. Development of pelagic oozes mainly composed of sand-sizedplanktonic foraminifera. Some fragments of larger echinoderms, molluscs, and bryozoa were transported to the site.
Silt-sized nannoplankton possibly winnowed out by same
currents. Secondary silicification and replacement of ooze
by chert in late Eocene or later.
Late Eocene to Late Oligocene
Nondeposition or very slight submarine erosion.
Late Oligocene to Late Middle Miocene

Figure 5. On-site sonobuoy profile at Site 209.

338

Further deepening of water and deposition of almost
pure foraminiferal ooze. Some marine currents transporting
shallower water benthonic foraminifera to site and winnowing out all but a small amount of nannoplankton.

SITE 209
TABLE 2
Coring Summary - Hole 209

Depth fromDrill Floor

Depth Below
Sea Floor

Cored

Recovered(m)

Recovery

9
9
9
9
9
9
9
9
9
9
9
9
9
9
9
9
9
9
9
9
9
9
9
9
9
9
9
9
9
9
9
9
9
9

9.2
8.4
9.0
8.2
6.8
9.3
0.0
0.0
0.5
0.0
0.0
0.0
0.0
2.1

100
93
100
91
76
100
0
0
6
0

2.4
1.1
1.0
0.0
1.5
0.7
0.0
3.0
1.3
1.5
0.0
1.9
3.9
0.6
0.0
0.8
0.2
0.0
2.3

0
0
23
11
27
12
11
0
17
8
0
33
14
17
0
21
43
7
0
9
2
0
26

301

76.7

25

Core

Date

Time

(m)

(m)

(m)

1
2
3
4
5
6
7
8
9
10
11
12
13
14
15
16
17
18
19
20
21
22
23
24
25
26
27
28
29
30
31
32
33
34

12/28
12/28
12/28
12/28
12/28
12/28
12/28
12/28
12/28
12/28
12/28
12/28
12/28
12/28
12/28
12/28
12/28
12/28
12/29
12/29
12/29
12/29
12/29
12/29
12/29
12/29
12/29
12/29
12/29
12/29
12/29
12/29
12/29
12/29

1010
1050
1130
1220
1255
1325
1415
1500
1545
1646
1730
1820
1900
1950
2035
2125
2245
2345
0050
0150
0255
0355
0450
0550
0625
0700
0745
0840
0925
1010
1120
1215
1310
1410

1438-1447
1447-1456
1456-1465
1465-1474
1474-1483
1483-1492
1492-1501
1501-1510
1512-1521
1521-1530
1530-1539
1539-1548
1548-1557
1569-1578
1588-1597
1606-1615
1625-1634
1634-1643
1643-1652
1652-1661
1661-1670
1670-1679
1679-1688
1688-1697
1697-1706
1706-1710
1710-1719
1719-1728
1728-1737
1737-1746
1746-1755
1755-1764
1764-1773
1773-1782

0-9

9-18
18-27
27-36
36-45
45-54
54-63
63-72
74-83
83-92
92-101101-110110-119131-140150-159
168-177
187-196
196-205
205-214214-223
223-232232-241
241-250250-259259-268268-272272-281281-290290-299299-308308-317317-326326-335
335-344

Total

(%)

0

1.0

Note: Echo sounding depth (to drill floor) = 1438 meters;
drill pipe length to bottom 1438 meters.

TABLE 3
Coring Summary - Hole 209A

Core

Date

Time

Depth fromDrill Floor
(m)

1

12/29

2130

1438-1447

Depth Below
Sea Floor
(m)

Cored
(m)

Recovered(m)

Recovery
(%)

0-9

9

2.2

24

Note: Only core attempted. Echo sounding depth (to drill floor) = 1438 meters;
drill pipe length to bottom = 1438 meters.

BIOSTRATIGRAPHY

Late Middle Miocene to Middle Pliocene
Nondeposition or very slight submarine erosion.
Middle Pliocene to Recent
Continued deepening of water to present 1438 meter
depth. Decrease in oceanic currents permitting higher
proportion of nannoplankton/planktonic foraminifera thanin the Miocene or earlier.

GeneralSite 209, which reached a subbottom depth of 344
meters, represents an incomplete late middle Eocene to late
Pleistocene sequence. Interpretation of the sequence issomewhat complicated by poor core recovery, the presenceof cherts, downhole contamination, and poorly preserved
microfossils at certain intervals.

339

SITE 209

Three factors of general interest are as follows: (l)The
presence of an unconformity representing the middle andearly Oligocene that is of regional significance, having also
been found in Sites 206, 207, 208, and 210. (2) A record of
substantial and possibly progressive deepening from the
middle Eocene to the late Pleistocene, due to tectonic
subsidence of this part of the Queensland Plateau. (3) The
presence of an excellent sequence of well-preserved, abundant calcareous microfossils of middle Pliocene to late
Pleistocene age.
The three following biostratigraphic units are recognizable, each separated by sedimentary breaks:
1) Late Pleistocene to middle Pliocene (209-1 to 209-5,
CC) containing abundant, well-preserved planktonic foraminifera and common, moderately preserved calcareous
nannofossils but lacking Radiolaria.
2) Late middle Miocene to late Oligocene (209-6-1 to
209-14, CC) containing abundant, moderate to wellpreserved planktonic foraminifera and low frequencies ofmoderately to poorly preserved calcareous nannofossils.
Radiolaria are also absent in this interval.
3) Late Eocene to late middle Eocene (209-15-1, 75 cm
to 209-34, CC) containing rather poor faunas of planktonic
foraminifera and rare, poorly to moderately preserved
nannofloras. Radiolaria are present in two samples of late
Eocene age.
Paleodepth Interpretation

Distinct upward deepening is evident within this middle
Eocene to Pleistocene sequence.
Middle to late Eocene sediments, in general, contain abenthonic foraminiferal assemblage—Discorbids, Polymorphids, Rectuvigerina, and Cibicides (compressed)—indicative of upper bathyal to outer sublittoral depths.
No deeper-water forms are present. Planktonic foraminifera
are much less abundant than in younger sediments, further
supporting the implied relatively shallow depths of deposition. Echinoid spines are common, and bryozoan fragments
occur in some samples. The presence of the characteristically neritic calcareous nannofossils Discolithina andBraarudosphaera, especially in the middle Eocene, represents further strong evidence of moderately shallow depths.
A gradual change to more open oceanic conditions in thelate Eocene is suggested by the gradual reduction of thesenear-shore calcareous nannofossils. An absence of Radiolaria, which are alsmot exclusively of open-ocean habitat, inthe middle Eocene can be attributed to the shallow-water
character of these sediments. Drilling at the previous sites
has demonstrated that Radiolaria are particularly abundantin sediments of this age, and thus their absence at this site isrelated to local conditions.
Reworked benthonic foraminifera occur in the late
Oligocene sediments, and depth analysis is difficult without
additional studies. The much greater abundance of planktonic foraminifera compared with underlying sedimentssuggests deeper, more open-ocean conditions. Very low
frequencies of calcareous nannofossils are probably due towinnowing by bottom currents.
Further deepening to the late middle Miocene is suggested by benthonic foraminiferal assemblages clearly340

indicative of upper bathyal depths {Planulina, Ehrenbergina, Textularia, Saracenaria, Pullenia bulloides, andhispid Uvigerina; lack of shallow-water forms; lack ofdeeper-water forms). Additional support for bathyal depths
is the presence of an abundant planktonic foraminiferal
fauna.
Pliocene-Pleistocene benthonic foraminifera (hispidocostate and hispid Uvigerinids; Gyroidina (large), Pleurostomella, Cibicides (rounded), Oridorsalis, and Eggerella;lack of shallower forms) reflect even further deepening tothat of the present day (approximately 1400 meters). Thus
considerable, and possibly progressive deepening, hastaken place from the upper bathyal or outer sublittoralconditions prevailing during the Eocene to the middle
bathyal depths of the present day.
Foraminifera

Site 209 represents an intermittent record of planktonic
foraminifera ranging in age from the Pleistocene to the
middle Eocene. The sequence from late Oligocene toPleistocene age is of tropical character, while assemblages of
Eocene age, although containing tropical elements, haveclose affinities with Eocene temperate faunas.
Three distinct episodes of sedimentation are separated
by disconformities as shown by the following:
Pleistocene to middle Pliocene containing abundant,
very well preserved planktonic foraminifera (209-1,
CC to 209-5, CC)(Disconformity)
Late middle Miocene to late Oligocene containing
abundant, moderate to well preserved planktonic
foraminifera (209-6-1, 66 cm to 209-14, CC). A large
sampling break exists between 209-6, CC and 209-10,
CC(Disconformity)
Late Eocene to middle Eocene (209-15, CC to209-34, CC) of rather poor biostratigraphic character
due to intermittent coring, poor recovery, presence ofchert horizons, poor preservation at several intervals,
and downcore contamination
The Pleistocene (Core 209-1 and Sample 209-3-5, 146cm) is fairly condensed as at Site 208 and probably reflects
the less prolific productivity of calcareous microfossils in
the lower latitudes of the southwest Pacific. As expected,
warm and cool cycles, although obviously present, are lessdistinct than at higher latitudes. The Globorotalia
truncatulinoides-Globorotalia tosaensis transition is complicated within Core 2 by oscillations in ratio of these twoforms.
The late to middle Pliocene (209-3, CC to 209-5, CC) isrepresented by approximately 20 meters of sediment and,like Site 208, contains extremely well preserved planktonic
foraminifera. Of particular biostratigraphic interest is the
Globigerinoides sacculifera fistulosus bioseries, clearly preserved throughout this Pliocene sequence. Elsewhere, thisbioseries is often poorly represented because of poor

SITE 209

preservation. The Pliocene-Pleistocene sequence is clearly of
tropical character.
No samples were recovered from an interval of assumed
foraminiferal sands between 54 and 83 meters, although
this interval almost certainly contains a rather condensed
sequence of early middle to late early Miocene age.
The middle early Miocene to late Oligocene is represented by a classical sequence of tropical forms including
such forms as Globigerinoides primordius, Globigerinoides
altiaperturus, and Globigerina angulisuturalis.
The Oligocene-Miocene boundary is marked by the lastappearance of G. angulisuturalis and the first appearance ofGlobigerinoides primordius and Globorotalia kugleri.
The late to middle Eocene planktonic foraminiferal
faunas are characterized by relatively low diversity andcloser affinities to the New Zealand sequence comparedwith the overlying Neogene. This possibly reflects a more
southerly location of this site of deposition during the
Eocene compared with the Neogene, related to northward
drift of Australia away from Antarctica since the middle
Eocene.
Calcareous Nannofossils

Nannofloras obtained at this site indicate the presence ofan incomplete late middle Eocene to late Pleistocene
sequence which can be divided into the following biostratigraphic units separated either by sedimentary breaks or, lesslikely, by highly condensed intervals: late Pleistocene toearliest late Pliocene (209-1-1 to 209-5, CC); mid Micoene
to late Oligocene (209-6-1 to 209-14, CC); late Eocene tolate mid Eocene (209-15-1 to 209-34, CC).
However, interpretation of this sequence of events was
not straightforward, being complicated by semicontinuous
coring, by lack of core recovery (Cores 7 and 8), by massive
downhole contamination (Cores 9 and 14), and by thepresence of cherts (core catchers of Cores 16, 19, 21, 22,
and 27).
Pleistocene (209-1-1, 35 cm to 209-3-2, 35 cm;
Nannofossil Ooze)
The Pleistocene sediments contain lower than usual
numbers of moderately preserved calcareous nannofossils.
Species present are: Emiliania huxleyi, Gephyrocapsa
oceanica, other Gephyrocapsa spp., Pseudoemiliania
lacunosa, Oolithotus antillarum, Cyclococcolithus leptoporus, Helicopontosphaera kamptneri, Rhabdosphaera
clavigera,Thoracosphaera heimi, Umbilicosphaera mirabilis,"Discoaster" perplexus, Ceratolithus cristatus, Syracosphaera pulchra, Scyphosphaera apstenii, Cyclolithella
annula, Anaplosolenia brasiliensis, Scapholithus ganerotus,
and Pontosphaera spp.
Calcareous nannofossil content of the Pleistocene
sediments of Hole 209 is lower than in the corresponding
sediments of other holes. However, the Pleistocene sediments contain high proportions of foraminifera. The
combination of these two factors suggests winnowing of thesediments has been occurring throughout the Pleistocene. A
generally tropical environment of deposition is indicatedfor Pleistocene sediments.
The Pleistocene sediments can be fitted to the zonal
scheme of Martini (1971) as follows: 209-1-1, 35 cm to209-1-2, 110 cm, NN21; 209-1-3, 35 cm to 209-1-3, 110
cm, NN20; and 209-1-4, 35 cm to 209-3-2,35 cm.

Late Pliocene (209-3-2, 110 cm to 209-5, CC;
Nannofossil-Foraminiferal Ooze)
The late Pliocene sediments contain common moderately preserved calcareous nannofossils. Species commonly present are: Cydococcolithina macintyrei, Discoaster brouweri, Discoaster pentaradiatus, Discoastersurvulus, Oolithotus antillarum, and "Discoaster" perplexus. Other species present in smaller numbers or as
isolated specimens are: Scyphosphaera sp., Thoracosphaera
heimi, Scyphosphaera apstenii, Pontosphaera cf. scutellum,
Pseudoemiliania lacunosa, Gephyrocapsa sp.,Helicopontosphaera kamptneri, Rhabdosphaera clavigera,Syracosphaera
pulchra, Umbilicosphaera mirabilis, other Pontosphaeraspp., Scyphosphaera campanula, Ceratolithus rugosus, andCoccolithus pelagicus. Reworked species include Discoasterchallengeri, Discoaster variabilis, Sphenolithus cf. abies,
and, in the 209-5-4, 35 cm to 20905, CC interval, very
sparse Reticulofenestra pseudoumbilica.
The late Pliocene/Pleistocene boundary is marked by ageneral increase in the number of calcareous nannofossils
present in the sediment, as well as the first downward
appearance of Discoaster brouweri. The increased calcareous nannofossil content persists throughout the late
Pliocene. The environment of deposition was tropical forthe majority of the late Pliocene, with some slightfluctuations to cooler marginal tropical conditions (209-3-2
to 209-4-1) for short periods.
The Late Pliocene sediments can be fitted into the zonal
scheme of Martini (1971) as follows: 209-3-2, 110 cm,
NN18; 209-3-3, 35 cm to 209-3-3, 110 cm, NN17; and2090304, 35 cm to 20905, CC, NN16.

Mid Miocene (209-6-1, 35 cm to 209-6, CC;
Nannofossil-Foraminiferal Ooze)
Taxa present in this interval, which contains moderately
well preserved, abundant nannofloras throughout, include:
Catinaster coalitus (base at 209-6-1, 110 cm), Coccolithus
cf. pelagicus, Cydococcolithina macintyrei, "Discoaster"
perplexus, Discoaster variabilis group, Helicopontosphaera
kamptneri, Reticulofenestra pseudoumbilica group, Scyposphaera spp., Spenolithus moriformis group, and Thoracosphaera. Also undoubtedly present are a number of
discoasters other than D. variabilis s.l., but unfortunately
they could not be specifically identified due to all thenannoliths being strongly overgrown. Under these circumstances dating these assemblages, which definitely lack both
Cyclicargolithus floridanus and Discoaster pentaradiatus,
more exactly than mid Miocene s.l. is difficult. However,
judging from the observed range of C. coalitus the 209-6-1
assemblages are probably correlative with the mid Miocene
4/4 Catinaster coalitus (NN8) Zone of Martini (1971),
whereas the underlying 209-6-2 to 209-6, CC assemblages
may be correlative with his mid Miocene 3/4 Discoasterkugleri (NN7) Zone.

341

SITE 209

Downhole Plio-Pleistocene (Core 9; Essentially
Foraminiferal Calcic Ooze)
Taxa present in one of several small "white fine lumps"
surrounded by "brown coarse matrix"—the dominant
lithology—in the core catcher include: Ceratolithus rugosus,
Cydococcolithina macintyrei, Discoaster brouweri, D.
pentaradiatus, D. surculus, D. variabilis, Gephyrocapsa,
Helicopontosphaera kamptneri, Pseudoemiliania lacunosa(dominant), Reticulofenestra pseudoumbilica group, andSpenolithus moriformis group. Clearly this assemblage,
which is abundant and moderately well preserved,
represents downhole caving from the overlying unconsolidated Plio-Pleistocene.
Early Miocene (209-10, CC to 209-12, CC;
Foraminiferal Calcic Ooze)
This interval, characterized by core catcher only
recovery, contains two distinctly different types ofassemblages. The upper type, obtained by crushingplanktonic foraminifera from the core catchers of Cores 10
and 11, essentially consists of very rare, poorly preserved
Coccolithus eopelagicus, Cyclicargolithus floridanus, Discoaster deflandrei, and Spenolithus moriformis group. Also
observed were single specimens of Coccolithus ovalis s.L,
Discolithina sp., Helicopontosphaera sp. cf. parallela(209-11, CC), and Spenolithus cf. belemnos (209-11, CC).
Judging from their sequential position (see below) and thepresence of D. deflandrei, these assemblages are ofundifferentiated early Miocene age. As in the underlying
sample, this interval includes rare objects resemblingaragonite needles.
The lower assemblage type, represented by a small("few") moderately well preserved nannoflora, occurs in
the core catcher of Core 12. Taxa present include:
Braarudosphaera floridanus, B. cf. discula, Coccolithus
ovalis s.L, Cyclicargolithus floridanus, Discoaster deflandrei,
Helicopontosphaera parallela, H. recta (highest occurrence),
Spenolithus cf. belemnos (lowest occurrence), and S.
moriformis. Despite a careful search Reticulofenestra
bisecta, Spenolithus ciperoensis, and Zygrhablithus bijugatus were not found. By lacking these taxa and containing
H. recta and S. cf. belemnos, this assemblage clearly is thatcharacteristic of the uppermost part of the Spenolithus
ciperoensis Zone (NP25) of Martini (1971). According toMartini (1971) this zone is of late Oligocene age and occurs
in the upper part of the stratotype Bormidian of Italy.
However, this particular sample (209-12, CC) and that
underlying (209-13, CC) also contain Globigerinoides
primordius, a foraminifera which, according to Blow (1969,
p. 223), has its first appearance very close (immediately
below?) to the base of the stratotype Aquitanian—thelowest Miocene stage. Attempts to extract nannofossils
from the stratotype Aquitanian have so far failed(Bramlette and Wilcoxon, 1967, p. 100; Edwards, 1971, p.
415), so for the purposes of Leg 21 reports the nannofossil
assemblage listed above is considered to be of early Miocene
1/5 age. Datum levels closely approximating the base of
Globigerinoides in Site 209 are top Helicopontosphaera
recta, top Reticulofenestra bisecta, top Zygrhablithus
bijugatus, and base Spenolithus cf. belemnos. Of these the342

writer considers top R. bisecta (209-13, CC) to be the mostreliable for, although prone to reworking, it is abundant,
distinctive, highly solution resistant, and ubiquitous
whereas the others have known environmental preferences.
Thin elongated objects similar to aragonite needles occur inthis sample.
Late Oligocene (209-13, CC; Calcic Foraminiferal Ooze)
This interval, represented only by the core catcher ofCore 13, contains a small ("few") moderately wellpreserved nannnoflora. Taxa present include: Braarudosphaera bigelowii, Coccolithus eopelagicus, C. ovalis s.L,
Cyclicargolithus floridanus, Discoaster deflandrei (lowest
definite occurrence), Helicopontosphaera obliqua (highest
occurrence), H. parallela (lowest occurrence), Micrantholithus flosi, Reticulofenestra bisecta (highest occurrence),
Spenolithus moriformis group, and Zygrhablithus bijugatus(highest) occurrence). Also observed were "aragonite"needles, Cyclococcolithina macintyrei (minor downhole
contamination), and a single specimen of Helicopontosphaera recta (shipboard identification only). In containing R. bisecta, lacking S. ciperoensis, and underlying the209-12, CC flora this assemblage is clearly correlatable withthe upper part of the late Oligocene 2/2 part of the
Spenolithus ciperoensis (NP25) Zone of Martini (1971).
This zone is recognizable in the upper part of the stratotype
Bormidian Stage according to Martini (1971). This
assemblage is probably also a correlative of the late
Duntroonian to early Waitakian Discoaster deflandrei Zone
of Edwards (1971).
An unconformity spanning most of the late Eocene andOligocene occurs between 209-13, CC and 209-15-1, 75 cm
judging by the undoubted biostratigraphic progress madebetween these samples. This feature, which is part of theregional Eocene-Oligocene unconformity also found at Sites
206 to 208 and 210, probably underlies 209-14, CC, but
this cannot be confirmed by the nannofossils due to themixed nature of the Core 14 assemblages (q.v.).
?Late Oligocene (209-14-1, 90 cm to 209-14, CC;
Calcic Silty Sand)
This interval, examined at 209-14-1, 90 cm and 209-14,
CC, contains small, variably preserved nannofloras in which
at least two distinctly different components can berecognized. The more abundant ("few") and better
preserved ("moderate") fraction, which clearly represents
downhole contamination, includes: Ceratolithus cristatus,
Cyclococcolithina macintyrei, Discoaster brouweri,
Gephyrocapsa, Pontosphaera discorporal, Pseudoemiliania
lacunosa (relatively common), Reticulofenestra pseudoumbilica, and Syracosphaera histrica. This Plio-Pleistocene
component is more conspicuous in the upper of the two
samples examined.
The second fraction, which is very rare and poorly
preserved, consists of Coccolithus ovalis si., Cyclicargolithus
floridanus, Discoaster deflandreii, and Helicopontosphaera
obliqua in 209-14-1, 90 cm and of Coccolithus ovalis s.L,
Cyclicargolithus floridanus, Helicopontosphaera obliqua,
Reticulofenestra bisecta, Spenolithus moriformis, andZygrhablithus bijugatus in 209-14, CC. This component is
considered here largely on the rather tenuous grounds of

SITE 209

floral similarity and the presence of the Oligocene species
H. obliqua, to be of similar, late Oligocene, age to the209-13, CC assembalge (q.v.). This conclusion is supported
by a definite, but shipboard only, recognition of the late
Oligocene to early Miocene species Triquetrorhabdulus
carinatus in 209-14, CC. The probable occurrence of a third
component is implied by the presence, in 209-14, CC only,of common ascidian sclerites and of occasional poorly
preserved Cyclococcolithina formosa, Discolithina sp., andMicrantholithus basquensisl. These taxa are characteristicof the underlying sediment (q.v.), and the presence of C.
formosa indicates an age not younger than early Oligocene.
The presence of this component is interpreted on the
grounds that the presence of common ascidian sclerites
probably indicates sediment redeposition from a shallower
environment, as reworking from older strata. This
interpretation is consistent with the recovery of late Eocene
1/5 sediments in Core 15, some 9 to 18 meters below
209-14, CC and with the implied presence of the regional
Eocene-Oligocene unconformity in that unsampled interval(see Core 13 above).
The assemblage components described above suggestthat Core 14 represents an intimate mixture of downhole
caved and in situ sediments. This conclusion is compatible
with the lithological description of this core.
Late Eocene (209-15-1, 75 cm to 209-27-2, 35 cm;
Sandy Foraminiferal Ooze and Limestone with Chert)
This interval is characterized by low core recovery due
to alternating hard and soft lithologies with the latter
having little cohesion. Wherever possible, the harder, often
cherty horizons and the immediately adjacent sedimentwere not sampled for calcareous nannofossils. Despite this,most assemblages extracted were poorly preserved andsmall ("very rare" to "few"); the only horizons from which
moderately common floras were obtained being thosebelow Core 22 where the chert content is less obvious. Taxapresent include: Braamdosphaera cf. discula; Coccolithus
eopelagicus; C. ovalis; Cyclicargolithus floridanus (base at
209-27-2, 35 cm; C. reticulatus (209-15, CC to 209-27-2,
35 cm range); Cyclococcolithina formosa (209-15-1, 75cm); C. protoannula (209-17-1, 80 cm); Discoastersaipanensis (209-15-1, 75 cm; D. sp. of tani group;
Discolithina multipora (top at 209-17, CC);D. obliquipons(top at 209-17, CC);Zλ pulcheroides (top at 209-18, CC);
D. sp., Helicopontosphaera lophota (top probably at
209-17-1, 80 cm; very sporadic); Micrantholithus basquensis; Reticulofenestra bisecta (base at 209-27-2, 35 cm);
R. hampdenensisl (209-17-1, 80 cm);R. placomorpha (topat 209-15-1, 75 cm); Spenolithus furcatolithoides (top at
209-33, CC); and similar nonbifurcating forms such as S.
moriformis; Zygolithus dubius (top at 209-25, CC; veryrare); Zygrhablithus bijugatus; and several different formsof rhabdolith stems. Also observed were rare ascidiansclerites (in 209-15-1, 75 cm; 209-17, CC; and 209-23, CC)and, only in 209-15-1, 75 cm minor mid Miocene or
younger downhole contamination (Cyclococcolithina macintyrei andReticulofenestra pseudoumbilica group).
Although these assemblages are small, they are also
diverse. This fact coupled with the variety and consistentpresence of warm neritic preferring taxa such as

Braamdosphaera, Discolithina, and Micrantholithus indicate
proximity to a neritic water mass. However, these taxa arepresent in relatively low numbers. For this reason an
open-water depositional site marginal to a broad shallow(epicontinental) platform seems more likely than deposition under truly sublittoral conditions. That a relatively
warm climatic regime prevailed during the deposition ofthis interval seems probable judging from the presence of
braarudosphaerids, discoliths, and a large spenolith plus thesparsity of zygoliths. Also conspicuously absent, although
not necessarily for climatic reasons alone, is the genus
Chiasmolithus.
Although making a good paleoenvironmental story
possible, these assemblage characteristics unfortunately
make the exact age of this interval distinctly more difficult
to determine. That it is of late Eocene age seems beyond
doubt since Discoaster saipanensis and Reticulofenestra
bisecta overlap throughout. Furthermore, the presence ofReticulofenestra hampdenensisl, rare Helicopontosphaera
lophota, and Zygolithus dubius and the absence ofHelicopontosphaera reticulata, Spenolithus predistentus,
and S. pseudoradians suggest a position within the late
Eocene 1/5 to 3/5. Refinement beyond this of the age or
zonal assignment becomes very subjective. For example,
opinions would vary as to whether the absence ofChiasmolithus oamaruensis and Isthmolithus recurvus (azygolith) reflects age or environmental factors. Consequently, for the purposes of this report, a late Eocene 1/5
to 3/5 (Kaiatan) age is adopted for this interval which, inbiostratigraphic terms, clearly conforms to both the
Reticulofenestra bisecta and Discoaster saipanensis (NP 17)
zones of Edwards (1971) and Martini (1971), respectively.
A late Eocene 1/5 (early Kaiatan) age would normally beapplied to these zones.
A small unconformity appears to separate this intervalfrom the immediately underlying sediments judging fromthe apparent absence in this sequence of assemblages
correlative with the mid Eocene 7/7 (late Bortonian toearly Kaiatan) Discoaster tani nodifer Zone of Edwards(1971). This conclusion is supported by coincident changes
in the hardness, clastic content, and sonic velocity of thesediments. However, from the nannofossil point of view, anelement of doubt exists due to the apparent presence ofminor downhole contamination from this interval in theuppermost part of the underlying interval (q.v.).
Mid Eocene (209-28-2, 35 cm to 209-34, CC;
Sandy Limestone Becoming Calcic Silty Sandstone)
This interval, also characterized by low core recovery,
contains diverse, poorly to moderately preserved, small(mostly "few") nannofloras. Taxa present include:
Braamdosphaera bigelowi; B. cf. discula; Chiasmotolithus
grandis (top at 209-31, CC); C. solitus (top at 209-28, CC);
Coccolithus eopelagicus; C. ovalis s.l.; Cyclococcolithina
foramsa; C. protoannula; Discoaster barbadiensis (top at
209-29, CC);Zλ saipanensis (base at 209-30, CC);Zλ sp. of
distinctus group; D. wemmelensis (209-33, CC range);
Discolithina multipora; D. pulchra (top at 209-28, CC);Zλpulcheroides; D. sp. Helicopontosphaera lophota; H.
seminula; Microantholithus basquensis; Reticulofenestra
hampdenensis (throughout interval); R. placomorpha

343

SITE 209

(throughout interval); Rhabdosphaera gladius (top at
209-29, CC); R. spp. (including parallel-sided stems);
Spenolithus furcatolithoides si. (throughout interval; nobifurcation of the apical spine evident); S. moriformis;
Zygolithus dubius; and Zygrhablithus bijugatus. Alsopresent, apparently as downhole contamination from theoverlying late Eocene, are rare Cyclicargolithus floridanus(209-28-2, 35 cm); C. reticulatus (209-28-2, 35 cm and209-28, CC); and Reticulofenestra bisecta (209-29-1, 85cm). The presence of these latter taxa is incompatible withthe cooccurrence of relatively common Chiasmolithus
solitus.
Definite evidence for direct deposition of this intervalfrom a warm neritic water mass is provided by the variety,relatively high abundance, and consistent presence of
braarudosphaerids and discoliths. The overall calcareous
nannofossil characteristics of this interval, particularly
those of high diversity and constant occurrence, indicate an
essentially open-water origin and thus imply a middle orouter sublittoral, rather than inner sublittoral, depositionalsite unless on-shore drift conditions prevailed. These
conclusions are consistent with the other paleontologicaland lithologic evidence available, for example, the highbenthonic versus planktonic foraminiferal ratio; the absenceof both ascidian sclerites and radiolarians; and the highly
clastic, glauconite-bearing, essentially noncarbonaceous
nature of the sediments.
In containing C. solitus, R. hampdenensis, R. placomorpha, and R. gladius throughout and lacking both C.
reticulatus and R. bisecta, the 209-29, CC to 209-34, CCpart of this interval is clearly correlative with the mid
Eocene-6/7 (early and mid Bortonian) combined Discoasterdistinctus and Reticulofenestra hampdenensis zones of
Edwards (1971) and with the Chiphragmalithus alatus(NP 15) Zone of Martini (1971). The age of the uppermost,
209-28-2 to 209-29-1, part of this interval is more difficult
to determine due to the presence of anomalous taxa (seeabove). For the purposes of this report their occurrence isconsidered to be totally due to contamination from theoverlying strata. However, there is a very real possibility
that the occurrence of R. reticulatus is not due tocontamination. If this is so, then Core 28 must be
considered correlative with the mid Eocene 7/7 (lateBortonian to early Kaiatan) Discoaster tani nodifer zones of
Edwards (1971) and Martini (1970; NP16).
Siliceous Microfossils

Although cherts are frequent in almost all late Eocene
cores at this site, siliceous microfossils occur only in Cores
23 and 24. Studies on thin sections of the chert show thatforaminifera are the most important organic component
present. Sponge spicules are rare and partly dissolved andare probably the origin of the silica of the cherts at this site.
Radiolarians are rare in Cores 23 and 24. Their
preservation is moderate, many specimens being broken due
to the impact with the abundant sponge spicules withwhich they cooccur. In fact, the latter are so abundant thatthe sediment looks like a spongolite. Such an abundance ofsponge spicules is almost certainly related to rather shallow
water conditions in the Eocene at this site. Radiolarians344

present include: Calocyclas hispida, C. turris, Lychnocanoma sp., Thyrsocyrtis triacantha, Podocyrtis cf. argus, andTheocαmpe mongolfieri. Such an assemblage is indicative oflate Eocene age.
PHYSICAL PROPERTIES
Density and Sonic Velocity

Core reocvery at Site 209 was relatively poor, so it isdifficult to present a coherent picture of the physicalproperties of the rocks sampled. Reasonably continuous
data were recorded for Cores 1 through 6 and again near
the bottom of the hole (see summary). The physicalproperties results largely support the tripartite division of
the sequence cored, adopted on the basis of lithology (seelithology report).
Unit 1, consisting of late Oligocene to Pleistocene
foraminiferal and nannofossil oozes, has densities in therange 1.56 to 1.88 gm/cc and sonic velocities of about 1.59
km/sec. As will be seen from the other site reports, these
are typical densities and velocities for these lithologies atthese shallow subbottom depths.
Unit 2, consisting of sandy foraminiferal ooze, silicified
limestone, and chert of late Eocene age, probably has
densities in the range 1.9 to 2.3 gm/cc and velocities
ranging from 3.0 to 5.8 km/sec. Core recovery was very
poor and data are sparse. It is clear that only the hard partsof the unit were sampled and that both density and velocity
are highly variable.
Unit 3, middle Eocene calcareous sandstones and sandy
siltstones, is marked by a drop in velocity and density
between Cores 27 and 28. Density falls into the range 1.8
to 2.0 gm/cc, and velocities drop to 1.91 to 2.39 km/sec.
The drop in density presumably reflects the increase in theclay and detrital mineral content of these very impure
limestones and the concurrent rise in porosity, as opposedto the very dense, low porosity, highly silicified sedimentsof Unit 2.
Thermal Conductivity and Heat Flow

Measurements of thermal conductivity by the needle
probe method on cores to depths of 50 meters below
bottom (Cores 1 through 6, inclusive) gave relatively
uniform values, about 2.8 ± 0.2 m cal/°C cm sec
uncorrected for ambient pressure and temperature at thesea floor. Values are slightly higher below 30 meters depth
than above, which is most obviously explained bycompaction. The relatively high values are typical ofcarbonate oozes which are relatively low in water content.
Useful data for heat-flow measurements were obtainedon two attempts to measure downhole temperatures at thissite. At 27 meters depth, a relatively steady temperature of
4.84 ± 0.05°C was measured over several minutes after thestart of coring. Before that, the temperature remained quite
steady at 3.70 ± 0.02°C, suggesting that the instrumentation may have prematurely entered the core barrel, showing
an increased temperature only after the warmer sediments
had been cored. At 54 meters depth, the measurement was
somewhat ambiguous. The temperature during bottom
penetration was relatively steady at 7.1 ± 0.2°C, whereas

SITE 209

that during coring was equally steady at 7.5 ± 0.2°C. It is
possible that the coring disturbance in this instanceintroduced additional heat to the sediment.
Assuming a bottom water temperature of 3.70°C, as
recorded during the steady portion of the measurement
before penetration at 27 meters depth, the temperature
gradient to 27 meters is 0.042°C/m. On the other hand, themeasurement at 54 meters gave an overall gradient of
0.063°C/m. The heat flow values in the two instances are
1.2 and 1.8 HFU (µ cal cm~ 2 sec- 1 ), respectively. These
are within the range of normal values. The difference would
be reconciled if the bottom water temperature were 2.4°C,
and in this case the gradient and heat flow would besomewhat higher than normal.
SUMMARY AND CONCLUSIONS

Drilling at Site 209 on the edge of the Queensland
Plateau penetrated 344 meters, sampling three lithologic
units. Unit 3, from 308 to 344 meters, is glauconite-bearing
calcareous silty sandstone to sandy siltstone of late middle
Eocene age. Terrigenous detrital sands and silts compriseover 50% of the sediment. Microfossils in this unit indicate
deposition in upper bathyal to neritic depths. Unit 2, from150 to 308 meters, consists of detrital-rich foraminiferal
ooze and chert of late Eocene age. Core recovery was poorin this section due to the interbedding of the hard chert andsilicified limestone with unlithified foraminiferal ooze.
Approximately 10% to 30% of the sediment is composed ofquartz, feldspar, minor glass, and authigenic (?) glauconite.
Unit 1, from 0 to 150 meters, is made up of foraminiferal
ooze and nannofossil ooze of late Oligocene to Pleistocene
age with a break in the sequence from late Middle Miocene
to middle Pliocene. Winnowing is evident throughout thesection, but is most conspicuous prior to late middle
Miocene.
The regional unconformity occurs at Site 209 between
Units 1 and 2 and extends from late Eocene to late
Oligocene. The unconformity is not closely approximatedby reflector in the seismic profiles. The most prominent
reflector above basement (Reflector 4) crops out along theseaward margin of the Plateau near 2000 meters depth andhad previously been interpreted as an unconformity
surface. This is now identified as a late Eocene chert
horizon. The boundary between Units 2 and 3 isgradational.
A rough acoustic basement rises to 0.38 sec subbottom
at this site. This is calculated as 387 meters below the sea
floor based on the velocities in Units 2 and 3. The site
survey by the Kana Keoki shows this basement reflector asa faint rather smooth horizon at depths up to 1.0 sec
beneath portions of the Plateau adjacent to the site. This
reflector becomes deeper and cannot be traced on theseismic profiles near the margin of the Plateau.
The sedimentary record indicates that the Queensland
Plateau has undergone net subsidence from upper bathyal
to neritic depths in the middle Eocene to mid-bathyal
depths (near 1500 m) at the present time. During late
Eocene, as deepending progressed and oceanic circulation
established itself over the shelf, oceanic pelagic sediments
began to predominate.
Terrigenous detrital input decreased, and to a major
extent ceased, by late Eocene. Unit 1 has less than 5%

terrigenous component compared with 10% to 30% in Unit
2 and over 50% in Unit 3. Development of reefs and cayson the central Plateau during middle Eocene may haveblocked bottom transport and impeded current distributionof the land-derived sediments at that time. Alternatively,
development of the Queensland and Townsville Troughs,
narrow deeps isolating the plateau from the Australian
mainland, may have resulted in terrigenous debris failing toreach the Plateau.
REFERENCES
Blow, W. H., 1969. Late Middle Eocene to Recent planktonic foraminiferal Biostratigraphy: Intern. Conf. Plank.
Microfossils, Geneva, p. 199.
Bramlette, M. N. and Wücoxon, J. A., 1967. Middle Tertiary Calcareous Nannoplankton of the Cipero Section,
Trinidad, W. I.: Tulane Stud. Geol. v. 5, p. 93-131.
Edwards, A. R., 1971. A calcareous nannoplankton zonation of the New Zealand Paleogene: Planktonic Conf.,
2nd Rome 1970, Proc, p. 381-419.
Ewing, J. I., Houtz, R. E., and Ludwig, W. J., 1970. Sediment distribution in the Coral Sea: J. geophys. Res., v.
75.
Martini, E., 1971. Standard Tertiary and Quaternary calcareous nannoplankton zonation: Planktonic Conf., 2ndRome 1970, Proc, p. 739-785.
Williams, H., Turner, F. J., and Gilbert, C. M., 1954.
Petrography, an introduction to the study of rocks inthin sections: San Francisco (W. H. Freeman Co.), p.
406.
NOTE CONCERNING THE APPENDICESThe appendices consist of tables of shore laboratory determinations of grain size, carbon content, and mineralogical composition, summary visual descriptions of the cores
recovered from the site, photographs of the cores and, finally, an overall summary of the results of drilling at the site.
The symbols used to represent lithology in the core summary forms are explained in Chapter 2 of this volume. The
lithologic description of each core contains typical resultsof shipboard examination of smear slides of each lithology.
In order to make the lithologic descriptions more complete
we have also included many of the shore laboratory results.
These are identified by being placed in square brackets.
APPENDIX A
Grain Size Determinations, Site 209
Core, Section,
Top of
Interval
(cm)

Depth
(cm)

Sand

Silt

Clay

(%)

(%)

(%)

Classification

1-4,116.0
2-4,110.0
3-4,110.0
4-4,110.0
5-4,110.0
6-5,110.0
9-1,136.0
14-2,110.0
15-1,104.0
23-2,116.0
28-2,78.0
29-1,133.0
31-1,122.0
34-2,96.0

5.7

14.6
23.6
32.6
41.6
52.1
75.4
133.6
151.0
243.7
283.3
291.3
309.2
337.5

39.9
38.7
29.7
26.5
29.4
42.1
68.7
96.9
91.3
43.3
21.7
31.1
73.2

19.1
17.1
20.9
22.7
25.7
38.2
21.8

41.0
44.3
49.5
50.8
44.9
19.7

Sandy clay
Sandy clay
Sand-silt-clay
Sand-silt-clay
Sand-silt-clay
Silty sandSilty sand
Sand
Sand
Sandy silt
Sand-silt-clay
Sand-silt-clay
Silty sand
Clayey silt

1.1

1.2
4.8

9.5
1.9
3.9

43.3 13.4
49.6 28.7
46.0 22.8
15.4 11.3
63.0 35.9

345

SITE 209

APPENDIX B
Carbon-Carbonate Determinations, Site 209
Core, Section,
Top of
Interval(cm)
1-4,86.0
2-4,86.0
3-4,86.0
4-4,86.0
4-6,0
5-4,86.0
6-5,86.0
9-1,116.0
14-2,86.0
15-1,86.0
23-2,86.0
27-2,60.0
28-2,78.0
29-1,133.0
31-1,122.0
32-1,125.0
34-2,113.0

Depth
in HoleCarbonTotal

Organic
CarbonCaCO,,

(m)

(%)

(%)

(%)

5.4

10.9
11.2
11.5
11.3
11.3
11.4
11.1
11.5
10.1

0.0
0.0
0.0
0.0
0.0

90
93
96
94
94

9.9

0.0
0.0
0.0
0.1
0.0

95
92
95
83
83

7.0
9.5
7.1
5.6
3.1

0.1
0.1
0.2
0.2
0.3

58
78
58
45
23

3.9
3.5

0.4
0.4

29
26

14.4
23.4
32.4
34.5
41.4
51.9
75.2
133.4
150.9
243.4
274.1
283.3
291.3
309.2
318.3
337.6

APPENDIX D
Thermal Conductivity Measurements, Site 209

346

Core,
Section,Interval
Below
Top (cm)

ThermalConductivity(mcal/°C cm sec)

Standard
Deviation

Ambient
Core
Temperature(°C)

1-3,752-3,75
3-3,704-3,705-3,70
6-3,700.002771
0.002719
0.002783
0.002907
0.003016
0.002575

0.005465
0.004725
0.004810
0.009094
0.008416
0.008451

22.25
23.61
22.15
21.76
21.01
23.61

RemarksAPPENDIX C
X-ray Mineralogy Determinations, Site 209
Sample Depth
Below Sea
Floor
(m)

Diff.

0-9
9-18
18-27
27-36
36^5
45-54
74-83
131-140150-159241-250272-281281-290290-299308-317317-326335-344

5.6
14.7
23.7
32.7
41.7
52.2
75.3
133.7
151.0
243.6
274.1
283.3
291.3
309.2
318.3
337.5

53.7
51.5
50.4
50.7
51.3
52.9
53.6
47.6
52.8
68.3
62.6
67.8
66.1
77.6
77.2
73.3

27.7
24.3
22.5
22.9
23.9
26.5
27.4
18.1
26.3
50.5
41.6
49.7
47.0
64.9
64.4
58.2

2-20µ Fraction
23241-25027272-28128281-29029
290-29931308-31732
317-32634
335-344

243.6
274.1
283.3
291.3
309.2
318.3
337.5

97.7
87.8
84.1
73.2
81.4
82.2
79.3

96.5
80.9
75.1
58.1
70.9
72.2
67.7

57.8
12.4
13.3
38.2
23.6
22.9
22.8

5.6
14.7
23.7
32.7
41.7
52.2
133.7
151.0
243.6
274.1
283.3
291:3
309.2
318.3
337.5

85.0
90.9
97.2
87.9
90.6
98.6
98.9
92.7
91.7
90.1
91.2
86.7
88.5
89.2
87.6

76.6
85.7
95.6
81.0
85.3
97.9
98.2
88.6
87.1
84.5
86.3
79.2
82.0
83.1
80.6

11.7
12.8
14.9
11.0
12.4
15.5
10.9
8.3
7.1
2.0
1.5
5.1
1.7
1.5
1.6

Core

Cored
Interval
Below Sea
Floor (m)

Calc.

Quar.

99.1
99.7
100.0
99.6
99.5
99.6
100.0
100.0
92.7
98.6
82.6
68.9
62.6
35.5
40.4
91.1

0.9
0.3

Cris.

K-Fe.

Plas

Mica

Mont.

Trid.

Clin.

Pyri.

Kaol.

Amph.

Chlo.

Apat.

Bulk Sample
1
2
3
4
5
6
9
14
15
23
27
28
29
31
32
34

0.4
0.5
0.4

4.3
1.4
3.8
8.6
15.2
16.1
12.4
2.3

3.1
Pres.
9.1
10.9
2.8
24.4
26.1
2.8

4.2

17.1
58.8
50.1
5.8

39.8
41.4
33.2

3.3

4.3

4.6
10.1
10.1
8.6
1.8

14.9
4.6
6.7
25.4
17.0
17.6
17.4

2.1
3.8
4.3
0.7

0.9
2.1
2.4

4.5
S.I
0.6
5.7
4.7
0.8

1.9
1.5
1.5

0.7
1.1

0.5

10.2
17.8
13.5

3.0
8.1
4.3
6.4
6.9

6.6
6.5
6.7

6.3
12.1
18.9
3.8
3.7
6.5

1.2
2.5
1.7
1.6
2.2

1.2

<2µ Fraction
1
2
3
4
5
6
14
15
23
27
28
29
31
32
34
a

0-9

9-18
18-27
27-36
36-45
45-54
131-140150-159241-250272-281281-290290-299308-317317-326335-344

U-3 peak at 3.23 A.
U-l peak at 12.1 A.

b

-J

20.0
12.0
2.8
3.1
11.7
1.9
3.2

28.4
68.5
63.3
21.6
64.2
64.3
64.8

2.4

1.8
7.5
0.9
0.7
0.9

13.5
14.2
19.3
19.9
18.5

4.9
8.4
2.5
2.3
8.3
3.3
2.0
2.3

50.0
38.4
37.4
38.8
41.9
58.7
35.1
33.7
62.3
11.1
9.6
23.5
11.6
15.5
10.5

12.7
14.6
16.5
27.6
24.0
25.7
6.1

1.7
1.6

15.0
14.9
17.4
16.9
13.4
16.2

0.9
1.2
5.9
1.1
2.2

2.4
1.4
1.6
1.6

3.2

—

-

-

-

-

-

-

-

-

-

-

-

-

-

-

42.3
15.0

9.6

-

7.8

I

_

5.5
5.9

Trace

4^
00

Site 209

Hole

Core 1Site 209

Cored Interval: 0-9

HoleCore 2

Cored Interval: 9-18 m

FOSSILCHARACTER
LITHOLOGIC DESCRIPTION

LITHOLOGIC DESCRIPTIONNANNO BEARING FORAM CALCIC OOZEAND FORAM RICH CALCIC NANNO OOZE
Very pale orange (10YR8/2) - grayish
orange (10YR7/4) creamy, homogenous.
Insoluble residue -v.5% quartz and feldspar.

CALCIC RICH FORAM NANNO OOZF AND
NANNO FORAM OOZE
Homogeneous, creamy, very paleorange (10YR8/2 - grayish orange(10YR7/4).
60-40% forams plus angular carbonate (probably broken
forams and authigenic c a l c i t e )40-60% nannos
trace of carbonate spicules

20* forams
80* nannos

Large amounts of very f i n e d e t r i t a lmaterial at Section 3, 35 cm.

mineral

35* angular carbonate grains (mainly foram) fragments
HI l°àrn2l
Shipboard lab about 95 CaCO3

trace of zeolite crystals
parallel extinction R.I. <l.56
trace of carbonate spicules[93% CaC03][90% CaCO3][403; sand, 19% s i l t , 41% clay][X-ray - 28% amorphous, 72% crystalline:I
99* calcite, 1% quartz

40% clay and larger sized angular calcite
20% forams
20% nannos

CoreCatcher

53% nannos
45% forams

FORAM NANNO OOZE

[96% CaCO3]

Shipboard lab 96% CaC03[39% sand, 17° s i l t , 44% c l a y ]IX-ray - 24% amorphous, 76% c r y s t a l l i n e : ]I
99% c a l c i t e , 1% quartz
1
Moderate yellowish brown (10YR5/4)
streak of FELDSPAR BEARING FORAM RICHNANNO ASH
Glass is d e v i t r i f i e d .
Feldspar "-Abs An5

Site209

Hole

Core 3

Cored I n t e r v a l : 18-27 m

FOSSIL T
CHARACTER
_,
ö

B

d

o

.

l±.

=C

Q_

I

I

I
o

£

LITHOLOGY

Site 209

I

I
=j

|

3

Q

—i

LITHOLOGIC DESCRIPTION

UJ
o

Hole

Core 4

I FOSSIL I
oCored Interval: 27-36 m

I I

CHARACTER
I I

°

d

o

^

S

m

ë

1
5

N

N

R

"^~•-x-PiI-r"1"; J-R.TIT- _i_ f j 7T 1

M

LITHOLOGYCALCIC RICH NANNO. FORAM OOZEAND FORAM NANNO 0(17F
Homogeneous, creamy v e r y
l i g h t gray N8 to white N9.

i-i-O-" "-,-'

N

M

N

F M

--"-?• ~ " ': J . J I - ~ r — _!_:>< " T'
I J . " " - ^ -

_ _|
_

r-S
N

F M

üj

g

EMPTY

F M

l5c-~T"-j_i_~L
1.0— ‰ ~ r r j . ~ ' •_o._-|-L^_i

40X nannos
39% forams
20% carbonate unknown origin
CALCIC RICH FORAM NANNO OOZEAND NANNO FORAM OOZE
Homogeneous, creamy,

I K L - - f "I"'white N9

— F>_1_- "_r"
I o L - J - '1-o-i-" "-^
Shipboard l a b 99% CaC03

N

C M~rc•_,NF M

I ~^~•~-rPαi
_ —YT
D O
- -t-r^Dcà
1 "-4_r~r|_oj

50% forams
29% nannos
10% carbonate~r

DDE- » C3C3 i

- i

C M

N

50% forams
30% nannos^ % carbonate, unknown o r i g i n-)--J--~Po^fo r- - i - _ j α o-J- ^S=Fα^ 4- j _ -i f^Jr~_1_"_c:lαc:3

LITHOLOGIC DESCRIPTION

l

1

|

N

N CM

- •'-'J-^-π
*

S

tli

Z fi-~r-ij_~X- r S • E " ^""^_α|•—l -i~

10S0.540? forams
60* nannos° - -"-w.-rllI J- Pt .-r ' •- _i_^-j —p ' 1. D " T T

R M

TT]

o £
S 5

"

N R M

I

2

50% carbonate, unknown o r i g i n
25% forams
25% nannos

-]DD

^

3

Shipboard lab
determination 99% CaC03

i
rt> F~> *^―T" O O-

UJ

45% carbonate
30% forams
25% nannos

o

2

N

F M

- -'I , ~M ç f ^ j

S

NFM-Jr-£L'-L- , -1

- , " _ α α i : :

^ |

S

N F M

r^u^a.;~1

I •~1"- I ~- 1 -" L "I _~T^ t - _ u J ~T «-j_J~~-r~1*- -I- •_r^i_•J-_jL.
-'~»- - i 1 =1 j=ix.^-.!.
- . o
_i_
I-~o^jJ^•

4
N

N

C M

F M

60% nannos
38% forams-,r
GZ
L96% CaC03]
XM[30% sand, 21% s i l t , 49% clay]|X-ray - 23% amorphous, 77% crystalline:]'
100% calcite
I

- y

N

F

M

-S^l-^J--

<ß
I

N R M

-

-*^o

»t J-

-

Pl~-L-

~1"

N

C M

;

•_i_"_-r

= ^ i

$
A

K

"

J!
G

N

~ no- -, - ^Catcher

FM[94%CaC03]:°I- L I-" r -

N CM

2 0 %

f o r a m s

N

C

M

_Jj-J-

20% carbonate

F

A

G

69% nannos^y.••~--IJl1"lα^~j."1"-.><-l-^-L-J-

Eg>ll-r"
6

1

core

C
C

-i-

:πpj.• u.

?
F[26% sand, 23% s i l t , 51% clay]l×-f•ay - 23% amorphous, 77% crystalline:!
'
99% c a l c i t e , 1% quartz
I

60% nannos
20% carbonate, unknown

1

6
C M

XM

^«cac°3^

j_

N c M

N

iSSSS t.

- P« -1- - T .

N FM: ° - ^ V ;I'

60% nannoscc- α - r - -L-~
o~J-~i'-^'-• H^-i-_~o _l__ ^"i-,-L
I-itjL. _l_~L•_|_•J

Jgh>±:

CCD^- i t -1— - ' α >- , - —p.

ou - ~ 'Corei £ -J- -~T".
Catcher ??~-i-~ T["f~-LT~-T-l

I

455S
forams
44% nannos
10% carbonate

__^

O

O

Site 209

Hole

I
S

Core 5I FOSSIL I
CHARACTER
I I
°
=i a
. £

UJ
o

U-

=C

Cored I n t e r v a l ; 36-45 m

I

I

~]

2
LITHOLOGY

O.

Site 209

I I
o
S
|

^
5
S

Cl

•~

g

UJ
g

LITHOLOGIC DESCRIPTION

HoleCore 6FOSSIL I
I
CHARACTER
1 I
<=
£
ri
Q
. Pj
"
<p
u-

ca
<

EMPTY
1

1
F M

B ^ T • "_1_"
I =»-"!-, - Mr - i . _Z \j\~-_i_-NFI ^^.T-L.-

M

60% forams
37% nannos
2% other carbonate- ."**_if" T~ ~*~ i |r —r- ~1~_Lr-~'~—r

50% forams
43% nannos$% other carbonate

63% nanπos
25% forams
10% carbonate unknown o r i g i n
NShipboard lab 99% CaC03- j f -~1"- - , _ p -~ 1 "-!. .
- o _T_ - 1 -

N A M

3

CALCIC RICH FORAM NANNO OOZEAND NANNO FORAM OOZE
Homogeneous, creamy w h i t e , N9.

A

M

_ y T

forams
39% nannos
10% carbonate

cS~r

.

5
i

N

=-L.-T-r~ r
I_LJr -T~ : -Ljp~1"-^

A M

£

GZ

- i-H-Z-r"

9% carbonate

×M[29% sand, 26% s i l t , 45% c l a y ]|X-ray - 24% amorphous, 76% crystalline:]I
99% calcite, 1% quartz
I

*

ü
G

-

Core

-

5 m

_i_r T~ • • - J L T I -i-' x
40% forams
4 M

5nannos

N A M

20% carbonate

forams
45S nannos
5% other carbonate-^iT•T^jcc[92;; caco3].-i-^p-r.,-'GZ[42% sand, 38% s i l t , 20% clay]--"~-i-r_-r.
Z.._j_r~π- fa— H"1"A

NANNO FORAM OOZE
Homogeneous, creamy yellowish gray (5Y8/1)['Hü 3]

S^•ILTT-T

I YZrT-r-~r^ \L_~\T-T- ' «T_I_V-T

Shipboard lab 9B°i CaC03

60* forams
40% nannos: i-HrZ"r

r.
tu ;
|
g z • ?

£^3^;
I.•~.T•-

J! • L -Mi- r - j - -J • _ u r - T _ - -_LL_~r_r

£

~ -

_

,

Shipboard lab 99% CaC03

1

I ^=|.~r-—,—_1_--MT__T-.

=•j.-T-r^

ë= fc-rV±- CC1i33£_r-~r~_l_'

_

- •

5 0 X

ii^B
NAM

N A M

- i^T

- ^L--^r-r.
I ^-5i ~f~~T~
3c J r *_- °c -J^T

I I

!!
f
R

I—
—•

LITHOLOGIC DESCRIPTION: v••* ~ ~ r •Q 5_
i r_p-T*.
- ^ r~T; U_ f~f-r•- o .~T_ ."*"_
^

ε

uj
α

m

_1_

N

u
S

LITHOLOGY

o
P
f

TH
^
f
5i

^
] B-![ T

I

I

cc
a.

N A M
-

H

Cored Interval.- 45-54 m
I

67X nannos
30% forams-Mr-r-~r.
- ->-±r
-T
_ -i_
~r •
- j _
f—-T"

Catcher
5

!

c

«

ü

Ix-ray - 27% amorphous scattering, 73% crystalline:!
I
99.6% calcite, 0.4% quartz
I

rnrp

5 5 %

- L -~ L r-" T "-r

RF * ? Catcher J ^ r l x
II | | | |[- -Thr__-rJ

foranis40% nannos
5% other carbonate

65% forams

I

I

to
o

83-92able

58% c a r b o n a t e g r a i n s
39% forams
2% nannos

Core
Catcher

S i t e 209

DEFORMATION I

-r4.•

Core

80% forams
15% c a r b o n a t e unknown o r i g i n
5% nannos
NANNO BEARING CALCIC FORAM OOZE

C3 O
oo
iQi

Core 14cX

METERSSECTIOoPRES.

FOSSIL

ZONE

AGE
µ
G

LITHOLOGIC DESCRIPTION

Cored

Interval:131-140

LITHOLOGY

LITHOLOGICDESCRIPTION

LITHOLOGY

T_

3OQ O

CatcherT"

CD O CJ *DEFORMATION |Cored I n t e r v a l : 92-101

LITHO..SAMPLE |PRES.

ABUND.

ZONEFOSSILNot determinable.

R
A

LITHO.SAMPLE |PRES.

METERSABUND.

SECTIONFOSSIL
Hole

EMPTY

0.5-

1

LITHOLOGIC DESCRIPTIONN

84% sand and s i l t s i z e carbonate
15% forams
FORAM RICH CALCIC OOZE

R

M

1 . 0 - T"
T
T

2

|

AGE

p

Core
Catcher

si
+J

•°

N
F
R

F
A

P
G

1 1 1 1 | 1 1 1 1 |1 1 1 1

NF
R

METERS

CorellSECTION

Hole
FOSSILCHARACTER

N5-N6

M
G

FOSSILCHARACTER

Site209

1 MIDDLE EARLY MIOCENEFALITHOLOGY

FORAM CALCIC OOZE

Not determ(MIDDLE EARLY

c

NP25 (lower)p

R

LATE OLIGOCENETERSDEFO MAT

ABUN
R

Σ

LITHOLOGIC DESCRIPTION

LITHO

FOSS
N

LITHOLOGYN
F
R

LATE OLIGOCENE

IOC

,TI0

ONE

_,

z

o

DEFORMATION j

Cored I n t e r v a l :Cored I n t e r v a l : 110-119 m

LITHO.SAMPLE |Core 10FOSSILCHARACTER

Core 13Hole

LITHOLOGIC DESCRIPTION

50% forams
40% c a r b o n a t e unknown o r i g i n
5% nannos
NANNO BEARING CALCIC FORAM OOZEDEFORMATION J

Holezi α 1-4.1
α xz
iD C
a α <~r ' i-D o ~rCore

LITHO.SAMPLE

S i t e 209

lumps.

LITHOLOGY

Catcher

FOSSILCHARACTER

AGE*From w h i t e f i n e g r a i n e d

ZONE

S i t e 209

Cored I n t e r v a l : 101-110 m

METERS[X-ray - 27% amorohous, 73% c r y s t a l l i n e : !
1
100% c a l c i t e
1
65% sand and s i l t s i z e carbonate
30% forams
5% nannos
NANNO BEARING FORAM CALCIC OOZE

M
G

PRES.

Very pale orange (10YR8/2).
[95% CaC0 3 ][69% sand, 22% s i l t , 9% c l a y ]FA

ABUND.

ooc

CALCIC OOZE

5% nannos

1"~T

NANNO BEARING FORAM

NP25 (upper)

11 1 11 11 I I11 11 1Core
Catcher- JOO><z> «=>

r-

50% c a r b o n a t e
45% f o r a m s

N
F
R

FOSSIL

M*
G

A
A

CC
XM
GZ

ZONE

N
F
R

N

AGE

LITHOLOGIC DESCRIPTIONEMPTY

V Pc cf 4Core 12FOSSILCHARACTER

CORES 7 & 8 : NO RECOVERY

1

Hole

SECTIONS i t e 209

EARLIEST MIOCENE (WAITAKIAN)

LITHOLOGY

DEFORMATION

ZONE

AGE
DOWNHOLE ENTIRELY ("PLIO-PLEISTOCENE")

α:α_

Cored I n t e r v a l . 7 4 - 8 3 m
LITHO.SAMPLE

Lo re 9FOSSI LCW RAC FERMETERSHoleSECTIONS i t e 209

CoreCatcher

T
T
T
T
T
T"
T
-r•

Rllill

92-76% carbonate c r y s t a l s ;5-20% forams
2% nannos
2% glauconite

4

some authigenic c a l c i t e has
scalenohedron c r y s t a l s as overgrowths of f i n e r grain c a l c i t e
and forams.

FORAM RICH SILTY CALCIC SAND
F r i a b l e , l i g h t greenish gray (56Y8/1)
Largely cavings.

CC
GZ
XM

[83% CaC03][97% sand, 1% s i l t , 2% c l a y ]CALCIC SILTY SAND

N
F
R

R

F

P

C

M

P

1

DEFORMATIONMETERSSECTIONPRES.

ABUND.

N

LITHOLOGY

1 1 1 1 | 1 1 1 1 | I 1 11

R. bisecta (NP17)FOSSIL

ZONE

AGE

Cored I n t e r v a l . 1 5 0 - 1 5 9 m

Site 209

LITHO.SAMPLE ||Core 15
FOSSILCHARACTERLATE EOCENE (KAIATAN)

50% f o r a m s

4CCo 1O * ò H
j IM«a 1 A 1 A

Corel7

Hole

Cored I n t e r v a l : 187-196 m

LITHOLOGIC DESCRIPTION

LITHOLOGIC DESCRIPTIONFORAM, S I L T Y CARBONATE SAND

45% carbonate, unknown
Homogeneous, y e l l o w i s h grayo r i g . including(5Y8/1)c a l c i t e overgrowths
on forams and f i n e grainc a l c i t e grains[83% CaC03]

60% forams
34% carbonate(lime mud 8 cement)
2% g l a u c o n i t e
1% feldspar + quartz

2% feldspar

y e l l o w i s h gray (5Y8/1) - l i g h t o l i v e gray (5Y6/1)
c h e r t - o l i v e gray (5Y4/1)

CHERT AND C H E R T y

LIMEST0NE

Light o l i v e gray (5Y6/1)
X-ray - 26% amorphous, 74% c r y s t a l l i n e :93% c a l c i t e , 4% quartz, 3% c r i s t o b a l i t eCoreCatcher

GLAUCONITE BFARTNG FORAMLIMESTONE AND SILICIFIED LIMESTONE CHERTFORAM LIMESTONE REPLACED BY
IRREGULAR SECONDARY CHERTSILICIFIED ECHINODERM, FORAM BEARING SILTY
SANDY LIMESTONE
Hole

Cored I n t e r v a l : 196-205 m

Core 18

DEFORMAT ION

METERSSECTIOABUND.

PRES.

ZONE

FOSSILLITHOLOGIC DESCRIPTIONAGE

FOSSILCHARACTER
LITHOLOGY

LITHO.SAM

Site 209

Cored Interval: 168-177 m

LITHOLOGIC DESCRIPTION

EMPTY
0.5 —

1

GLAUCONITE BEARING FORAM RICH
SILTY LIMSTONE, SILICIFIED LIMESTONEAND CHERTLight olive gray (5Y6/1);
chert is olive gray (5Y4/1).
Pr

M

S i t e 209

Hole

Q

F
R

CatcherCore 19F OSSI L
CHA RAC rER

σ

Core

•=C

C

(X

M

Core
Catcherl a b 93% CaC03

FORAM LIMESTONE AND SECONDARY CHERT

Cored I n t e r v a l : 205-214 m

LITHOLOGY

H

grayforams
Shipboard;f|Tyfi;

DEFORMATION

F

r

45%

LITHO.SAMPLE

LATE EOCENE (N

METERSQUARTZ, VERY FINE SAND AND SILT BEARINGAND FORAM RICH LIMESTONE: SILICIFIED
AND REPLACED BY CHERT.

_SECTIONI
VIV>I

This is a foram-rich calcarenite (Foram andlime mud grains cemented by calcite) thatby drilling was broken into sand and s i l t
size grains that show overgrowths of clear
calcite cement over original clastic grains
and fossils.
Shipboard lab 33% CaC0 3

QUARTZ SAND AND GLAUCONITE BEARINGFORAM LIMESTOME; CHERTY e l l o w i s h gray (5Y8/1) c h e r t - o l i v ez
R. bisecta (NPl

Shipboard lab 47% CaC0 3

A a r tf ΛTÒ
1 . 0 - ~B ti Φi •iàli H* 1 1* A fi* 1 9

ZONE

77% carbonate
crystals &grains20% forams
2% glaucoπite

AGE

HoU

R. bisecta (NP17)

Site 209

1 LATE EOCENE (KAIATAN)

toLITHOLOGIC DESCRIPTIONQUARTZ SAND AND GLAUCONITE BEARINGFORAM LIMESTONE; CHERTl i g h t o l i v e gray (5Y6/2)
c h e r t - o l i v e black (5Y2/1)

P

C

M

R

F

fi

Hole

Core
Catcher

No a r t i f i c i a l grading or sorting by d r i l l i n g .
May represent soft interbeds between hardcherty layers.

F

S*

S*

F

METERSSECTION

PRES.

[43% sand, 43% s i l t , 14% clay]
X-ray - 51% amorphous scattering, 49°< crystalline:!
98.6% c a l c i t e , 1 A% quartz
1
FORAM AND NANNO BEARING SPONGESPICULE RICH CALCIC OOZEα oα D c?" α o oS* 3 α α cCore 2ΦABUND.

FOSSILZONE?. bisecta (NP17]

Forams, and minor echinoderms and mollusca
are cemented by sparry c a l c i t e withscalenohedron shaped c r y s t a l s ; volcanic
glass - l i g h t R.I. <l.56

AGE

QUARTZ SAND AND GLAUCONITE BEARINGFORAM LIMESTONE! CHERT
limestone - very l i g h t gray (N8) yellow gray (5Y8/1)
chert - o l i v e gray (5Y4/1)[58% CaC03]*
CC

Cored I n t e r v a l : 250-259

LITHOLOGY

DEFORMATIONC

F

Cored In terv al . 532-241 m

GLAUCONITE BEARING QUARTZ S I L T , NANNO
AND FORAM-RICH SPONGE SPICULE*
CALCIC OOZE

1

46% carbonate crystals
25% forams
25% sponge spicules
2% nannos
1% glauconite
U radiolaria

1.0— .: s * . - . . - . .

N

C

P

F

C

M

R

R

G

Core
Catcher* ^;. s *c A S*AGG A A A

GLAUCONITE-NANNO BEARING FORAM AND
SPONGE SPICULE OOZE; CHERT IRREGULARLYREPLACING SPONGE SPICULE LIMESTONE

LITHOLOGY

C^Δ, Δ Δ Δ

(P|

Δ A

»
Δ Δ Δ
0 . 5 - £^λ Δ Δ Δ

1
1.0-

N

R

P

F

A

M

R

Core
Catcherθrr_) G GG
Vtf G G N (G G G G C G
N G G G G (DEFORMATION

cc
ct_

LITHO.SAMPLEzoU-METERSQUARTZ SAND AND GLAUCONITE BEARINGLIMESTONE; CHERTl i g h t o l i v e gray (5Y6/1)
c h e r t - o l i v e gray (5Y4/1)

SECTION

Cored I n t e r v a l : 2 5 9 - 2 6 8 m

F DSSI L
CHA RAC rER
ZONE

DEFORMAT

LITHOLOGIC DESCRIPTION

AGE

Core
Catcher

LITHOLOGY

LITHOLOGIC DESCRIPTION

EMPTY

0.5-

R. bisecta (NP17)-*

LITHO.SAMPLE

1 1 1 11 1 1 1 1 1 1 1 1 1

DEFORMATION?
•2

LATE EOCENE(KAIATAN)

1 1 1 11 ] 1 1 1 1 1 1 1 1>

LATE EOCENE (KAIATAN)R

NANNO BEARING FORAM AND SPONGE SPICULE*
RICH LIMESTONE
creamy, homogeneous, y e l l o w qray (5Y8/1) l i g h t o l i v e gray (5Y6/1)§
SECTIOABUND.

PRES.

F

S

FOSSIL

Catcher

Co re 22N

CHARACTER

LITHO.SAM-

Hole

FOSSIL

ZONE
R. bisecta (NP17)

AGE

S i t e 209

Core-

METERSR. bisecta (NP17)

LATE EOCENE (KAIATAN)R

LITHOLOGIC DESCRIPTION

EMPTY

F

FOSSILCHARACTER| LATE EOCENE KAIATAN)

LITHOLOGY<t

1

Site 209

Cored I n t e r v a l . 223-232 m
LITHO.SAMPLE]

METERSSECTION

ZONE

AGE

u_

DEFORMATION
2

1.0F

LITHOLOGIC DESCRIPTIONLIMESTONE (BIOSPARITE) IRREGULARLY REPLACEDBY CHERT
limestone - l i g h t o l i v e gray (5Y6/1)
c h e r t - o l i v e gray (5Y4/1)

S*

1

2

o

LITHO.SAMPLE

METERS
0.5-

P

F

N

2

S*

Core 21

FOSSI LCHPRAC rER

LITHOLOGY

A A^A ACore
Catcher

Hole

Cored I n t e r v a l : 241-250 m|
SECTIONPRES.

ABUND.

FOSSILZONE

1.0-

R. bisecta (NP17)1Core 23|
QUARTZ SAND AND CLAUCONITE-BEARINGFORAM LIMESTONE CHERT
limestone - l i g h t gray (N7)chert - o l i v e gray (5Y4/1)
A r t i f i c i a l graded bedding produced by d r i l l i n g .
Only hard layers preserved in c h i p s . Softintervening layers probably s i m i l a r but
u n l i t h i f i e d foram oozes.

4

0.5-

R

LITHOLOGIC DESCRIPTION

AGE

P
P

Hole
FOSSILCHARACTERLATE EOCENE (KAIATAN)

R

DEFORMATION 1

F

LITHOLOGY

LITHO.SAMPLE |Q_

R

METERS

ZONE
R. bisecta (NP17)

LATE EOCENE (KAIATAN)

cC

N

SECTION

1AGE

F DSSI L
CHA RAC1 ER

σ

Site209

Cored I n t e r v a l : 214-223 m

Hole|

Site 209

LITHOLOGIC DESCRIPTIONLIMESTONE; CHERT
chert - o l i v e gray (5Y4/1)
FORAM CALCIC OOZE

Shipboard lab
determination 88% CaC03
50% carbonate c r y s t a l s(sparry c a l c i t e ,broken shell f r a g ments)
45% forams
1% nannos
2% quartz and feldspar
λ% glauconite

GLAUCONITE-NANNO BEARING FORAM RICHCALCIC OOZE
semi l i t h i f i e d greenish gray (5GY6/1)

W
O

Hole

Co -e 26

Cored

EMPTY

Core
Catcher

G CW CG G t G G G
G G G G GC
G G ( G G G
G G G G G I
G G ( G G G
G G G G G (G G G G G G
G G G G G (G G^~P) G G
N Lj>G G (G G G G G N
G G G G G (NANNO AND GLAUCONITE BEARING SANDYCALCIC FORAM OOZE AND L I T H I F I E D L I M E STONE EQUIVALENTCC

L78i CaC03J
XM

Shipboard lab 68" CaCO3

greenish gray (5GY6/1)
32%

c a r b o n a t e

55! nanπos
2% glass
2% quartz & feldspar+ Cristobalite &tridymite
1% glauconite

determination 82% CaC03
X-ray - 42% amorphous s c a t t e r i n g , 58% c r y s t a l l i n e : ]83* c a l c i t e , 4% quartz, 9% C r i s t o b a l i t e ,4% t r i d y m i t eJMicrocrystalline c a l c i t e cements
f o s s i l s and d e t r i t a l grains.
Chert f i l l s forant chambers and voids.
GLAUCONITE-NANNO SILICEOUS SPICULE BEARINGCALCIC'FORAM OOZE <Z% d e t r i t a l quartz sandmicroxln. c a l c i t e cement; chert f i l l s voids
and replaces f o s s i l s . Sponge? spicules havesecondary overgrowths of chalcedony.

Core
CatcherSite 209

Hole

Core 29

F 3SSI L
CHA RAC ER

o
cc
α.

u_

+

II
-*J

^

Cored Interval:290-299

LITHOLOGY

0.5 —DEFORMATION

G c |r, G G (G G li G G Gfc>C 'C, P~~^ I

LITHO.SAMPLE

M

Insoluble residue subangular grains
50% quartz
15% glauconite
Tourmaline? inclusion 10% feldspar
in quartz, d e v i t r i 10% l i g h t glass
fied glass, altered
3% dark glass - yellowish
feldsparbrown R.I. >l.56
2% amphibole
5% clayG ;&£:%: F.

METERSA

X-ray - 50% amorphous scattering, 50% crystalline:• 69% c a l c i t e , 9% quartz, 11% C r i s t o b a l i t e ,5% Plagioclase, 5% tridymite, 1.9% c l i n .

DESCRIPTIONSECTIONR[22% sand, 50% silt, 28% clay][68% CaC03]

LITHOLOGIC

ZONE

F

GLAUCONITE BEARING, SAND-RICH FORAH LIMESTONE
Laminated, s l i g h t y mottled
greenish gray (5GY6/1) to grayish
o l i v e (10Y4/2).

r : .

AGE

2

VERY FINE GRAINED QUARTZ SAND, GLAUCONITE,
FORAM AND NANNO BEARING CALCIC CHALKl i g h t α r e e n i s h qrav (5GY8/1) and SILICIFIEDLIMESTONE e q u i v a l e n t l i g h t gray (N7)

ON IAN)M

LITHO.SAf PLE

DEFORMAT ION

LITHOLOGY

1 1 I I1 1 1 1 1 1 1 M 1C

LITHOLOGIC DESCRIPTION

LITHOLOGIC DESCRIPTIONI n terv al:272-281 m

d±2G
NCHARACTER

MIDDLEMETERS1

R. bisecta (NP17)

Cored

1 1 1 11 1 1 I I 1 1 1! 1

PRES.

ABUND.

FOSSILZONE

AGE

SECTIONLO re 27

FOSSILCHARACTERLATE EOCENE(KAIATAN)

111

CatcherR

Hole

S i t e 20?

LITHOLOGY

DEFORMATION

PRES.
P
M

METERSABUNO.
FA

SECTIOFOSSILAGE

ZONE
R. bisec(NP17

LATE EOC(KAIATANF

H

FOSSILCHARACTER

LLJ

Cored I n t e r v a l ; 2 8 1 - 2 9 0 m

In terval:268-272 m

FOSSILLITHO.SAMPLE

j

Site 209

EMPTY

1
N

F

P

-5

1

0 GZ

CL
XM

α
N

C

M

F

C

M

R

LITHOLOGIC DESCRIPTIONGLAUCONITE-NANNO SPONGE SPICULE BEARINGSANDY FORAM RICH LIMESTONE
greenish grayT5GY6/l) to~ grayish o l i v e(10Y4/2), s l i g h t l y burrowed
35% carbonate (sparryc a l c i t e , microcrystall i n e cement)
25% forams
10% amphibole
5% nannos
5% glauconite
5% l i α h t glass R.I. <l.56
5% dark glass R.I. >l.56
5% quartz
5% feldspar[31% sand, 46% s i l t , 23% clay][45% CaC03]
L

Core
Catcher3J

fX-ray - 47% amorphous, 53% c r y s t a l l i n e :1
63% c a l c i t e , 15% q t z . , 3% c r i s . ,4% K-feldspar, 10% p l a g . , 2% mica,L
1% mont.. 1% t r i d y m i t e , 1% c l i n . J
Abundant secondary chert.

£ U.

R

GLAUCONITE-NANNO BEARING SILICEOUS SPICULE
RICH SANDY LIMESTONE
pale o l i v e (10Y6/2)
Insol.
25% quartz
5% feldspar
3% glass
4% glauconite
3% hornblende

i/> B
•o sz

S i t e 209

Core

R

Catcher

Hole

Core34

DEFORMAT ION

PM

LITHOLOGY

LITHO.SAI PLEF
CF

METERSPRES.

NSECTIOABUND.

Abundant secondary c h e r t f i l l i n g foram
chambers and voids. Has well-developedm i c r o x l n . c a l c i t e cement.

Core
Catcher

ZONE

LITHOLOGIC DESCRIPTIONFOSSILp

I n :erval:326-335 m

FOSSILCHARACTER

AGE

F

METERSCF

SECTIOABUND.

N

PRES.

ZONE

AGE
EOCENEB

LITHOLOGY

Cored

Co re 33

Hole

LITHOLOGICDESCRIPTIONGLAUCONITE SILICEOUS SPICULE BEARINGQUART7 SAND RICH FORAM LIMESTONE

X.FΠ;Cored I n t e r v a l : 3 3 5 - 3 4 4 m

1

1

MIDD

(BO O N I A N )C

FOSSILCHARACTERU

s i t p 209

Cored Interval:299-308 m

MIDDLL EüCEN(BORTONIAN)
D. distinctus
R. hampdenens

Core 30

FOSSIL

DEFORMAT ON

Hole

LITHO.SAM PLE

S i t e 209

LITHOLOGIC
Core 31

METERSLITHOLOGY

11 1 1 1 1

SECTIOPRES.

ABUND.

FOSSIL

F

P

F

R

P

Core
CatcherR

DESCRIPTIONGLAUCONITE SILICEOUS SPICULE NANNOBEARING QUARTZ SAND RICH FORAM LIMESTONE
dusky yellow green (5GY5/2) to gray olive
green (5GY3/2), slightly to moderately
mottledShipboard lab 35% CaC03

EMPTY

m
i

[1% sand, 63% silt, 36% clay]
GZ
CC
XM

GLAUCONITE NANNO BEARING QUARTZ SAND
RICH FORAM LIMESTONE[73% sand, 15% s i l t , 11% c l a y ]-ray - 58% amorphous scattering, 42% crystalline
51% calcite, 13% qtz., 15% cris.,
10% plag., 4% mica, 4% tridymite,
3% clin.

[23% CaCO3][26% CaC03][X-ray - 65% amorphous s c a t t e r i n g , 35% c r y s t a l l i n e : " !
36% c a l c i t e , 16% q t z . , 24% c r i s . ,10% p l a g . , 4% mica, 2% mont.,
L
6% t r i d y m i t e , 1.5% d i n . , 0.7% amphibole J

In thin section microcrysta-line calcite
cements forams, detrital quartz, Plagioclase
and siliceous sponge spicules.
Secondary chert (micro×ln. quartz,
christobalite and tridymite) f i l lforam chambers and voids.

grayish o l i v e(10Y4/2)

Shipboard lab
determination 43% CaCO3

Cored Interval;317-326 m
DEFORMATION 1PRES.

FOSSILABUND.

LITHOLOGIC DESCRIPTION

Cored I n t e r v a l : 0-9 m

LITHOLOGY

LITHO.SAMPLE |Core 1

METERS

Hole
FOSSILCHARACTER

CHARACTERSECTIONS i t e 209A

FOSSILAGE

MIDDLE(BORT
D. dist inctus +R. hamp denensis(-NP15)o(NVINO
3N3003N

LITHOLOGIC

ZONE

ZONE

AGE

FOSSILCHARACTER

1DESCRIPTION

Cored I n t e r v a l : 308-317
UEFORMAT ON

Hole

LITHO.SAMPLE

S i t e 209

LITHOLOGIC DESCRIPTIONo1

50% nannos
49% forams
1% z e o l i t e s

1 . 0 - r-~r•FELDSPAR AND QUARTZ SAND BEARING FORAMLIMESTONECoreCatcherdusky yellowish green (5GY5/2) tograyish olive green (5GY3/2), slightly
burrowed

FORAM NANNO OOZECreamy, homogeneous,very pale orange (10YR8/2).

NN[29% CaC03]
X-ray - 64% amorphous, 36% c r y s t a l l i n e :40% c a l c i t e , 12% q t z . , 26% c r i s .
9% p l a g . , 4% mica, 2* mont.,
5% t r i d y m i t e , 1% p y r i t el i g h t o l i v e gray (5Y5/2) to gray o l i v e (10Y4/2)

2
N

|
•_L

_

N

Core
CatcherSS

SITE 209
0 Cm

25

50

75

—100

125

150

209-1-1
356

209-1-2

209-1-3

209-1-4

209-1-5

209-1-6

SITE 209150

209-2-1

_ -2
209 2

209-2-3

209-2-4

209 -2-5

209-2-6
357

SITE 209

0 cm

' fi

j

t

I

II

I

1
9

ij

1
1

25

1I

f

, |i

I1

1

I

i

•

>

j

-*

', !

I
50

J

1-3

i

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*
9

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-

75

<

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i

|

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!,

'1

:

100

I

!

:

1
•

|

I
!

:

1

1

125

i

|
!

j

I

i
•

)

209-3-1
358

j

i

s

j

•

I

i

1

fi

150

J

!

1

;

i

1

209-3-5

209-3-6

H•••

i

1

209-3-2

209-3-3

209-3-4

SITE 209

0 cm

25

50

75

100

125

150

209-4-1

209-4-2

209-4-3

209-4-4

209-4-5

209-4-6
359

SITE 209

0 cm

25

50

75

100

125

150

209-5-1
360

209-5-2

209-5-3

209-5-4

209-5-5

209-6-1

SITE 209150

209-6-2

209-6-3

209-6-4

209-6-5

209-6-6

209-9-1
209-14-1
36

SITE 209

0 cm

25

50

75

100

125

150

209-14-2
362

209-15-1

209-16-1

209-16-2

209-17-1

209-18-1

SITE 209

0 cm

25

50

75

100

125

150

209-20-1

209-21-1

209-23-1

209-23-2

209-24-1

209-25-1
363

SITE 209

0 cm

1

1
j

I'

)
:

1

•:

A

1

,"

J

: '.

' "'''~ j

V

./j

H

l•

1
9

J

1

i

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HI

HI

:

I 1

1

j'"

j

1

75

•

••'

fl

I

||

Λ

•

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II

H

f
"1
:

li

11

1
1

•
•

i

V

25

50

π

"1
—-

\ -i

I

1:

-1
1

1

•

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^ B

f

» 1

I
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•
•

100

•óé-J

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,

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SJ
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1

r

B••l

•
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j

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θ

L -1 ::

I|

1

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1. J

^i

ft 0 •' 1

j

150

1

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209-27-1
364

•

II

II

209-27-2

209-28-1

209-28-2

Λ _>..-^* « ., Jilt

H
"91

/

4
- \

j'

r

π

i

125

.j

II

NI

1

209-28-3

209-29-1

SITE 209

0 cm

— 25

50

— 75

—100

— 125

150

209-32-1

209-34-1

209-34-2

209A-1-1

209A-1-2
365

SITE 209

Density (gm/cc)

ON

AGE

LITHOLOGY

UNIT 1
PLEISTOCENE

NANNO BEARING CALCIC I ORAM OOZE and
FORAM RICH CALCIC NANNO OOZELATEPLIOCENE
MID
PLIOCENE
MID
MIOCENE-50

EARLY
MIOCENE

100

13
LATE
!_J_
OLIGOCENE
14

UNrr_i_
UNIT 2LATE
EOCENE150
GLAUCONITE BEARING SANDY I ORAM OOZE
and LIMESTONE
Silicified and irregularly replaced by chert.

-200

Sponge spicules.

250

1.00

1.50

2.00

2.50

Velocity (km/sec) and Impedence
3.00,1.00

4.00

7.00

(^―

10.00

. $—
13.00

SITE 209 c o n t .

*g
zc

AGE

8

D e n s i t y (gm/cc)_!
mJ~~2M ^LITHOLOGY

UNIT 2 (cont.)

1.00

1.50

2.00

2.50

""~

'

I

'

Velocity(km/sec) and Impedence

4JX)

7^00

3 . 0 0 1.00

( ^ _ . 2__)

10.00

13.00

'

25
2

r • F y ^ UNIT 2
27rr
UNIT 3

OΠ|E—in—1^O|-12___

29
h•
30

"*"
—.

Glauconite, ash, nanno and feldspar bearing, I 0 RAM AND QUARTZ RICH CALCIC SILTY SANDSTONE and SANDY SILTSTONE

-»

o

*

CD

-

-300
_

31

©
_

o

32

hI

L

| g A . •• • •

34
_J

L-^x

344 m Bottom of hole.

)

'

'

'

E9
o