10. SITE 210
The Shipboard Scientific Party1

Location: Coral Sea Basin
Position: 13°45.99'S, 152°53.78'E
Water Depth: 4643 meters
Total Penetration: 711 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: Graded cycles of silt and clay with interbeds of nannofossil ooze overlie a Miocene abyssal clay. Below this is an
Oligocene sequence of clay-bearing to clay-rich nannofossil chalk and clay-bearing calcic nannofossil chalk which overlies theregional unconformity (mid Oligocene/late Eocene). Clay-bearing calcic nannofossil chalk grades downward, with increasing
clay component, into clay nannofossil chalk to clay. The oldest dated sediment recovered is early Eocene in age.
BACKGROUND AND OBJECTIVESGeneralSite 210 was .initially proposed to investigate the age,history, and biostratigraphy in the Coral Sea Basin. Locatedroughly in the center of the Coral Sea abyssal plain, thenearest margin was sampled at Site 209 on the Queensland
Plateau, and the presumed major source of sediment in New
Guinea (Fly River region) is 450 miles to thewest-northwest.
Prior to site survey, information was available in theform of some seismic profiling and sediment sampling

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.

which had been conducted earlier (see, for example, Ewing
et al., 1970; Gardner, 1970) and preliminary location of thesite was on the basis of these data. Site survey was
conducted by the R/V Kana Keoki, and the site survey data
provided the basis for final selection of the site.
Review by the JOIDES Panel on Pollution Prevention
and Safety indicated that the site and drilling program weresatisfactory with continuous coring, moderate drilling
precautions, and standard abandonment procedures.
Site Survey

The region encompassing Site 210 was surveyed by R/VKana Keoki in September 1971. The sea floor (Figure 1) of
the Coral Sea Basin is quite flat with gradients generally lessthan 1 m/km. By contrast, the acoustic basement structure(Figure 2) is locally quite rough and the site is located overa basement high which has relief of 0.4-sec round-trip travel
time. The basement relief is not uniform throughout thebasin, but consists of a series of elevated structures such as
those on the tracks to the survey area.
A short distance east of the site (Figure 3), a tilted block
structure exposes some of the deepest sediments as a hill inthe basin. Although the basin sediments are generally wellstratified with two more highly reflective intervals, anear-basement "transparent" interval occurs which is
generally conformable to the irregular deep reflector.
Occasionally a deeper reflector is detected; normally steep

369

SITE 21054' -153β00'E

153β00'E
Figure 1. Bathymetry at Site 210 (uncorrected meters).
R/V Kana Keoki site survey, October 1971.

Figure 2. Acoustic basement (seconds of reflection time)at Site 210. Kana Keoki site survey October 1971.

slope problems are minimal. These patterns are most clearlyseen in the profile in Figure 3 where deeper elements are
uplifted.

signal return suggesting that major boundaries are not
involved or are obscured by structures and interference inreflections. Reflector 4 appears as acoustic basement athigh speeds southwest of the site and is generally horizontal
on the approach profile. Reflector 4 is clearest at low
speeds as a rough acoustic basement. It can also be seen in
the high relief region around Location 1000 on theapproach profile. Reflectors 1, 2, and 3 are horizontal andgenerally regular reflectors in the "abyssal plain" section on
all profiles, and they bound some of the previously
described transparent intervals (Ewing et al., 1970).

OPERATIONS
Site Approach

The site approach track (Figure 4) shows very clearly thereflective patterns of the survey profiles. At low speeds (5kt) for the initial site crossing and the beacon drop, theintermittent deep reflector is well defined. This profileshows more stratification than most in the area. This may
be a function of the frequency output of the paired 5-cu in.
and 30-cu in. air guns being towed. At the site the deepreflector rises to 0.8 sec subbottom. The transparent
horizon conforms to this lower surface, and there arehorizontal stratified reflectors above.
Sonobuoy
The on-site sonobuoy (Figure 5) does not present thesame general appearance of stratified and transparent
intervals as seen in the underway profile. The five principal
reflectors picked in the sonobuoy record are, however,clearly correlatable to the underway records. Table 1
summarizes the sonobuoy data and initial interpretation.2
The reflective horizons are generally weak to moderate in

Final correlations of sonobuoy profiles using laboratorymeasured velocities, other physical properties, and lithologic
boundaries are presented in Part II of this Initial Report.

370

Drilling Program

Fifty cores (Table 2) were attempted, and the first one
wa? on deck at 0005 on 31 December. A continuous coringroutine was followed down to 90 meters following whichan alternating wash-and-core routine was carried out to 542
meters depth below the sea floor. With increased
consolidation of the sediment by this depth, the wash andcore procedure had become impractical, and continuous
coring was resumed for the interval, 542 to 641 meters.
With some apparent decrease in consolidation and a desire
to reach basement, a wash-and-core routine was reestablished for the interval 641 meters to the bottom of the holeat 711 meters. Basement was not reached before theend-of-leg deadlin e forced conclusion of operations. The
last core recovered was at 0200 on 4 January and the hole
was abandoned at 1130 on the same day.
Four downhole temperature measurements wereattempted at Site 210, using the retractable in-corer probe.
One was successful and the other three were unsuccessful
due to instrument damage during the operation.

SITE 210

* πöFigure 3. Seismic profile on approach to Site 210. Glomar Challenger.

Figure 4. Seismic profile departing Site 210. Kana Keoki site survey.

LITHOLOGY

GeneralHole 210, drilled in a water depth of 4650 meters, wascontinuously cored to a depth of 90 meters below the sea
floor and semicontinuously cored from 90 to 711 meters.
Fifty cores were taken and 262 meters of sedimentrecovered. Summaries of each core are given in Appendix F.

The cored sequence can be divided into five lithologic
units. From top to bottom they are:1) Unit 1 (0 to 470 m)-graded cycles of silt and clay
with interbeds of nannofossil ooze (Pleistocene to mid
Miocene).
2) Unit 2 (470 to 521.6 m)-clay (mid Miocene to early
Miocene).
3) Unit 3 (521.6 to 540 m)-clay-bearing to clay-richnannofossil chalk and clay-bearing calcic nannofossil chalk(mid Oligocene to late early Oligocene).

371

SITE 210

4) Unit 4 (540 to 554.4 m)-clay-bearing to clay-rich
calcic nannofossil chalk with minor chert nodules (earlylate Eocene to mid Eocene).
5) Unit 5 (554.4 to 711 m)-clay nannofossil chalk to
clay (mid Eocene to late early Eocene).

SITE 210

Unit 1(Graded Cycles of Silt and Clay
with Interbeds of Nannofossil Ooze)

Figure 5. On-site sonobuoy pro
file at Site 210.

TABLE 1Site 210 Sonobuoy Data

Reflector

Depth
(sec)

1

0.20

2

0.42

3

0.52

4

0.65

5

0.80

372

NatureWeak, lowfrequency weak
Weak/moderate,
no low frequency
Moderate, no low
frequency
Moderate/strong,good low frequency,
general underway
acoustic basement
Weak/moderate, nolow frequency

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

1500

150

1500

315

1600

395

1800

512

2000

662

Approximately 1900 graded cycles of silt and clay
averaging about 14 cm in thickness occur in Unit 1. These
numbers were obtained from determinations in the portionsof the cores that are relatively undisturbed by drilling andthe total calculated by extrapolation for the disturbed coresand the uncored intervals. The bases of the cycles are
generally olive black to dark greenish gray silt and are often
in erosional contact with the underlying beds. Some of thebases are laminated and a few are cross-laminated.
Examinations of smear slides indicate that the basal
sediments of the cycles are composed mainly of quartz,
altered glass?, foraminifera, and feldspar. Minor constituents present in varying amounts include plant debris,
chlorite, mica, clay minerals, pyrite, and other opaques,zeolites, nannofossils, ascidian sclerites, and various
nonopaque heavy minerals (most commonly amphibole).
Bulk samples from near the bases of about 15 different
graded cycles were examined by X-ray diffraction, and theaveraged results show that the main components of thecrystalline phase are quartz (26%), calcite plus aragonite(22%), mica (21%), and Plagioclase (17%). The subordinate
components in decreasing abundance are chlorite, montmorülonite, kaolinite, amphibole, potash feldspar, andpyrite.
The middle portions of the graded cycles are generally
greenish gray clayey silts to silty clays composed mainly ofclay minerals and clay- and silt-sized detrital particles. Bulk
samples from near the middles of about 10 different gradedcycles were examined by X-ray diffraction, and theaveraged results are similar to those from the bases of thecycles. Calcite plus aragonite (29%), quartz (24%), mica(29%), and Plagioclase (14%) again compose about 85% of
the crystalline phase. Subordinate components are the sameas in the bases. Some of the middle portions, however, arenoncalcareous.
The upper portions of the cycles are generally lightgreenish gray clays composed mainly of clay minerals,
clay-sized particles, and nannofossils that are smaller andmore corroded than in the biogenic interbeds between
cycles. The darkness of the upper portions depends on theclay to nannofossil ratio. The more nannofossils present,
the lighter the color. Some of the upper portions aremottled by burrows. X-ray diffraction of bulk samples fromnear the tops of three different graded cycles yielded resultsthat are similar to those for the base and middle portions of
the cycle. Quartz (25%), mica (22%), calcite (21%), andPlagioclase (16%) compose about 85% of the crystalline
phase. The subordinate components are also similar to
those for the base and middle portions of the cycles exceptthat pyrite was not detected.
The graded cycles of silt and clay are interpreted asturbidites because of: (2) the presence of grading upwards

SITE 210
TABLE 2
Coring Summary - Site 210

Core

Date

Time

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
35
36
37
38
39
40
41
42
43
44
45
46
47
48
49
50

12/31/71
12/31/71
12/31/71
12/31/71
12/31/71
12/31/71
12/31/71
12/31/71
12/31/71
12/31/71
12/31/71
12/31/71
12/31/71
12/31/71
12/31/71
12/31/71
12/31/71
1/1/72
1/1/72
1/1/72
1/1/72
1/1/72
1/1/72
1/1/72
1/1/72
1/1/72
1/1/72
1/1/72
1/1/72
1/1/72
1/1/72
1/2/73
1/2/72
1/2/72
1/2/72
1/2/72

0005
0140
0255
0430
0545
0655
0825
0945
1110
1235
1350
1515
1650
1825
1945
2120
2215
0020
0200
0330
0510
0645
0820
1000
1130
1310
1600
1740
1930
2125
2305
0055
0255
0520
0805
1130
1405
1615
1800
2020
2220
0025
0245
0545
0755

min
1/2/72
1/2/72
1/2/72
1/2/72
1/3/72
1/3/72
1/3/72
1/3/72
1/3/72
1/3/72
1/3/72
1/3/72
1/4/72

UIO

1425
1800
2210
0200

Depth fromDrill Floor(m)

Depth Below
Sea Floor

Cored
(m)

Recovered(m)

Recovery(m)

4653-4662
46624671
46714680
4680-4689
4689-4698
4698-4707
4707-4716
4716-4725
4725-4734
47344743
4756-4765
4775-4784
4793480248124821
48314840
48504859
48684877
48874896
49064915
49254934
49444953
49624971
49814990
5000-5009
5018-5027
5037-5046
5056-5065
5074-5083
5093-5102
5112-5121
5130-5139
5149-5158
5168-5177
5186-5195
5195-5204
5204-5213
5213-5222
5222-5231
5231-5240
5240-5249
5249-5258
5258-5267
5267-5276
5276-5285
5285-5294
5301-5310
5318-5327
5331-5340
5345-5354
5355-5364

0-9

9

9-18
18-27
27-36
3645
45-54
54-63
63-72
72-81
81-90
103-112122-131140-149
159-168
178-187
197-206
215-224234-243
253-262272-281291-300309-318
328-337347-356365-374384-393403-412421-430440449459468477486496-505515-524533-542542-551551-560
560-569569-578578-587587-596596-605605-614614-623623-632632-641648-657665-674678-687692-701702-711

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

8.9
9.0
9.4
0.0
4.5
7.2
0.6
6.6
5.6
5.2
1.8
6.0
3.0
2.3

Total

(%)

9

5.4

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

5.4
4.0
3.6
8.4
4.0
2.9
4.9
4.5
3.8
8.7
4.4
5.6
4.4
9.4

99
100
100
0
50
80
7
73
62
58
20
67
33
26
17
11
22
6
27
61
44
70
100
100
62
0
89
86
72
44
100
92
94
60
60
80
64
44
40
93
44
32
54
50
42
97
49
62
49
100

450

262.3

58

1.5
1.0
2.0
0.5
2.4
5.5
4.0
6.3
9.4
9.4
5.6
0.0
8.0
7.7
6.5
4.0
9.2
8.3
8.5

7.2
5.8

Note: Echo sounding depth (to drill floor) 4650 meters;
drill pipe length to bottom 4653 meters.
from coarser to finer detritus; (2) their highly terrigenous
composition (especially the quartz, mica, Plagioclase, plantdebris, and heavy minerals; (3) the evidence of scour at thebase of many of the cycles; and (4) the abundance ofreworked shallow-water, benthonic foraminifera in thebasal portions of many cycles as well as the occasional
occurrence of ascidian sclerites, probably of shallow water,
benthonic origin.
Several ungraded, parallel laminated (minor crosslamination), fine sand, and coarse silt beds with sharp upperand lower boundaries occur throughout the interval. Thesemay have been deposited by oceanic bottom currents. If so,
the size of the detritus implies a relatively fast bottom
current of about 1 knot.
The laminated bases of some of the graded cycles may
have resulted from a succession of turbidity currents ofsubequal strength which successively eroded most of theprevious graded cycle, eventually producing a "laminatedbase" comprised of the basal portions of many individual
turbidites.

373

SITE 210

Using the same method of determination and extrapolation as for the graded cycles, it was calculated thatapproximately 800 interbeds of nannofossil ooze make up
about 15% of Unit 1. They have an average thickness ofabout 8.5 cm and occur between graded cycles of silt andclay. It is often difficult, however, to distinguish clay-richbiogenic oozes from the upper nannofossil-rich portions ofsome of the graded cycles of silt and clay. Most of theinterbeds are light greenish gray; but some are white andclay free whereas others are dark greenish gray and clay
rich. Many of the interbeds are mottled by burrows (someChondrites and Zoophycos types were recognized). Of thebiogenic component of the oozes, calcareous nannofossils
predominate with subordinate amounts of foraminifera.
Although the interbeds are largely of biogenic origin, many
may have been deposited by turbidity currents because of(a) the well-preserved nature of the calcareous nannofossils(the present water depth is 4650 m), (b) the evidence ofconsiderable reworking (in some cases indicating that morethan one source was being eroded), (c) the apparent size
sorting in some beds, and (d) the presence of small but
persistent amounts of ascidian sclerites of probable shallow
water, benthonic origin.
Twenty-seven measurements of organic carbon (insoluble carbon remaining after treatment with HC1) were madeon samples from Unit 1 and the average weight percent is0.5. This average is about five times higher than the
averages for the other units at Site 210. Organic carbon
percentages at all the other sites on Leg 21 also averaged
about one fifth that of this unit. These high percentages in
Unit 1 are consistent with the hypothesis of turbidity
current emplacement and relatively rapid burial of
terrigenous and shallow water debris in the deep sea.
If all the graded cycles of silt and clay are turbidites,
then turbidity currents carrying elastics were coming into
the Coral Sea Basin at the rate of about 1 per 5000 years
for about the past 10 million years. However, because someof the biogenic interbeds are probably turbidites, theoverall frequency of turbidity current influx into the Coral
Sea Basin is probably closer to about 1 per 4000 years forabout the past 10 million years.
Occasionally throughout Unit 1 there are subordinate
lithologies or sequences other than those already described.
A 55-cm-thick bed of foraminiferal ooze occurs at about
140 meters (Core 13). Nearly 3 meters of interbedded
nannofossil ooze and clay occur at 291 to 294 meters (Core21). About 8.5 meters of nannofossil clay underlain by 40
cm of calcareous sandy silt occur at 347 to 356 meters(Core 24). About 2.7 meters of nannofossil ooze occurs at
421 to 424 meters (Core 28). About 2.85 meters ofnannofossil ooze and interbeds of noncalcareous clay occur
at 440 to 443 meters (Core 29). All but 50 cm of Core 30
are nannofossil ooze and interbeds of clay.
The main conclusion drawn from the above as well asfrom the distribution and size of nannofossil ooze interbeds
is that about the lower third of Unit 1 is richer in biogenic
components and the upper two-thirds is richer in elastics.
The upper two-thirds of Unit 1 accumulated at a rate ofabout 70 meters per million years, whereas the lower thirdaccumulated at less than half that rate (about 30 meters per
million years).

374

The boundary with the underlying unit falls within an
uncored interval of about a dozen meters and has been
arbitrarily placed in the middle of the uncored interval.
Unit 2 Clay
Unit 2 is mainly composed of clay minerals andclay-sized particles and is subdivided into two parts:
Subunit 2A: 470 to 500.5 m. The sediment is mostly
dark greenish gray, slightly to moderately mottled,semilithified, noncalcareous clay with subordinate silty
clay. An X-ray analysis of a bulk sample at 480.1 meters
shows that the crystalline phase is composed predominantlyof mica (39%), Plagioclase (21%), and quartz (18%) withsubordinate amounts of montmorillonite (10%), chlorite,
potash feldspar, and amphibole. The <2 micron fraction isenriched in montmorillonite (27%). A microscopic
determination indicates that the mica is muscovite and the
Plagioclase is andesine. The upper 35 cm of the subunit
contain two 5-cm-thick beds of lighter greenish grayforaminiferal and quartz-rich calcic silt. A 7-cm-thickcarbonate bed occurs in the middle of the subunit at about
483 meters. The basal 1.3 meters of the subunit are olive
gray, indicating an increase in brown-colored detritus and atransition to Subunit 2B.
Subunit 2B: 500.5 to 521.6 m. The sediment isyellowish brown to dark yellowish brown, semilithified,moderately but indistinctly mottled clay with subordinate
silty clay. Rare small greenish gray patches occur. An X-ray
analysis of a bulk sample at 503.7 meters shows that the
crystalline phase is mostly montmorillonite (32%), quartz(19%), mica (16%), potash feldspar (15%), and Plagioclase(12%) with minor amounts of chlorite and kaolinite. The
2-20 micron fraction is enriched in quartz (30%), potash
feldspar (26%), and Plagioclase (21%) whereas the <2micron fraction is mainly montmorillonite (50%). Microscopically, the mica is muscovite and the Plagioclase isandesine, as in Subunit 2A. One 15-cm band of pale orange
to yellowish brown calcareous silt occurs just below 525
meters. It consists mainly of carbonate particles with asmall proportion of calcareous nannofossils.
Unit 2 is interpreted as an abyssal clay because of the
scarcity of biogenic sediment and the slow accumulation
rate of 4 meters per million years. The contact with theunderlying highly calcareous beds probably represents a
disconformity or a highly condensed sequence (seeBiostratigraphic Summary). The two lithologies areinterbedded over about a 15-cm interval.
Unit 3 (Clay-bearing to Clay-rich Nannofossil
Chalk and Clay-bearing Calcic Nannofossil Chalk)

The chalk of this unit is yellowish brown, yellowish
orange, and yellowish gray. It is semilithified andmoderately to intensely mottled with darker wisps
throughout, giving it a "bird's eye maple "-like texture.
Pinkish gray bands and patches occur in the lower part.
Four insoluble residue determinations on samples from
Unit 3 average 10%. This correlates well with two shorelaboratory determinations of calcium carbonate 3 content
which average 89%. An X-ray analysis of a bulk sample at533.7 meters shows that the crystalline phase is almost
entirely calcite (98%). The calcium carbonate-free residue

SITE 210of the <2 micron fraction is predominantly montmorillonite (74%) with subordinate clinoptilolite (12%), quartz,
mica, Plagioclase, and chlorite. Smear slide examination of
the carbonate component of the sediment suggests that asignificant proportion of fine nonnannofossil material ispresent. Scanning electron microscope examination shows
this to be small rhombs of authigenic calcite. The exact
nature of the boundary with the underlying Unit 4 isunknown because of a small gap in core recovery. However,the boundary lies within a few meters interval andrepresents a significant unconformity (see Biostratigraphic
Summary) that is of regional extent. Here the unconformity appears to be angular.
Unit 4 (Clay-bearing to Clay-rich Calcic
Nannofossil Chalk with Minor Chert Nodules)
The chalk is light olive gray to very light greenish graywith pinkish gray patches and lenses scattered throughout.
Minor glauconite occurs in the lower two meters. Unit 4 issemil?thified, moderately mottled, with a "bird's eyemaple "-like texture as in the overlying unit. The carbonate
consists of nannofossils and small calcite rhombs. Layering(? bedding) is inclined at about 20°. An insoluble residue
determination on a sample from Unit 4 is 9%, whereas two
shore laboratory determinations of calcium carbonate
content average 81%. Bulk samples from 547.7 and 551.7
meters were X-rayed, and the results show that calcite(95%) is the predominant component of the crystalline
phase with minor amounts of montmorillonite, quartz,
mica, and clinoptilolite. The calcium carbonate-free residueof the 2-20 micron fraction is mainly quartz (34%),
clinoptilolite (31%), mica (20%), and Plagioclase (14%)
whereas the <2 micron residue is predominantly montmorillonite (83%) with minor mica, quartz, clinoptilolite,
and Plagioclase. Chert occurs sporadically throughout theupper two-thirds of the interval as olive gray nodules up to
2 cm in diameter formed by replacement of the carbonate.
The contact with the underlying unit is gradational;
however, a distinct change in preservation of foraminifera
occurs at the boundary. Foraminifera in Unit 4 areparticularly poorly preserved, whereas they are moderately
well preserved in Unit 5 (see Biostratigraphic Summary).
Unit 5 (Clay Nannofossil Chalk, Calcic Nannofossil
Chalk, Nannofossil Clay, Calcic Clay, and Clay)The major constituents of this unit are calcareous
nannofossils, clay, and authigenic carbonate. The last has
been identified by scanning electron microscopy. These
three components are all present throughout in varying
proportions leading to a proliferation of lithologic names(eight in all are indicated on the core summaries). The
insoluble residue component of the interval, mainly clay
minerals and clay-sized particles, averages about 45%. Most
values are between 40% and 55%. These values compare
favorably with shore laboratory determinations of calcium
carbonate content, which average 53%, most ranging
between 45% and 60%. Clay and clay-sized particles
predominate in the lower part of the unit whereas calcite
predominates in the upper portion.
Unit 5 is semilithified, but is not as hard as the twooverlying units. From 627 meters to the bottom of the holeat 711 meters, short intervals of core have responded
plastically to drilling. These softer segments are morecommon below 651 meters. Bedding dips at 5° to 10°.
The unit can be broadly subdivided into three parts.
Subunit 5A: 554.4 to 570 m. The sediment is mainly
light greenish gray clay-rich calcic nannofossil chalk tonannofossil-rich calcic clay, moderately but indistinctly
mottled. Foraminifera are sparsely distributed throughout.
Bulk samples from 555.8 meters and 564.0 meters were
X-rayed, and the results show that calcite (79%) is the
predominant component of the crystalline phase withminor amounts of montmorillonite, mica, quartz, clinoptilolite, tridymite, cristobalite, and Plagioclase. The calcium
carbonate-free residue of the 2-20 micron fraction is mainly
quartz (33%), clinoptilolite (25%), mica (25%), andPlagioclase (14%) whereas the <2 micron residue ispredominantly montmorillonite (55%) with appreciable
amounts of mica (14%), cristobalite (14%), and quartz(9%). In the lower portion of Subunit 5A, darker
fine-grained pyrite is present in minor quantities inburrows.
Subunit 5B: 570 to 665 m. Lithologically this subunit issimilar to the above except that the color is very pale blue
green to light greenish gray and fine pyrite is much morecommon in burrows. The burrows are mostly surroundedby pale purple patches containing more sparsely distributed
pyrite. Bands several centimeters thick of the same hue arealso common. The coarse fraction of the insoluble residue
from a sample at 579.8 meters includes quartz, muscovite,
andesine, and albite. Nine bulk samples at approximately
10-meter intervals were X-rayed from Subunit 5B, and theaveraged results show that calcite (69%) is the predominantcomponent of the crystalline phase with subordinate quartz(14%) and minor amounts of cristobalite, mica, montmorillonite, tridymite, and Plagioclase. Cristobalite and tridymitewith one exception are found only in the upper half of thesubunit whereas quartz occurs throughout the interval.
However, in the upper samples in which cristobalite andtridymite occur, quartz averages only 4% whereas in thelower half of the subunit quartz averages 26%. Combining
the quartz, cristobalite, and tridymite percentages showsthat the silica content is rather constant (averaging 23%)throughout the subunit with its various phases being
significant variables. The calcium carbonate-free residue ofthe 2-20 micron fraction is mainly quartz (45%) withsubordinate critobalite (21%) and mica (18%) and minor
Plagioclase, potash feldspar, tridymite, chlorite, montmorillonite, barite, pyrite, and clinoptilolite. The <2 micron
residue is mainly quartz (37%), cristobalite (31%), andmontmorillonite (23%). Both size fractions of the residues
also contain cristobalite and tridymite in samples from theupper half of the subunit only. Foraminifera occur
scattered throughout most of Subunit 5B but increase infrequency at 635 meters where foraminiferal-rich bands
several centimeters thick appear, occurring at intervals tothe base of the subunit.
Subunit 5C: 665 to 711 m. The chalks and clays of thebasal subunit resemble those of the other two, but theburrows are filled with light olive gray sediment and pyrite
is much less common than in the overlying subunit. The
predominant colors of Subunit 5C are light bluish gray and375

SITE 210

light gray. Four bulk samples from the subunit were
X-rayed, and the averaged results show that in the
crystalline phase calcite (55%) and quartz (33%) predominate with minor mica, chlorite, montmorillonite, andplagioclase. The calcium Carbonate-free residues of the 2-20
micron and the <2 micron fractions are predominantly
quartz (73%) with subordinate mica (11%) and minor
chlorite (5%). Plagioclase (11%) is significant in the coarser
residue whereas montmorillonite (10%) is significant in thefiner residue. No cristobalite or tridymite were detected inthis subunit, unlike in the overlying subunit. Subunit 5C isforaminiferal-bearing throughout with foraminiferal-richbands from 704 meters to the base.
Sequence of Geologic Events Interpreted from Lithology

Early-Late Eocene
Accumulation of detrital clay and biogenic pelagic
sediment (nannofossils and foraminifera) took place in thelate early Eocene to the middle Eocene as represented by
Unit 5. The accumulation rate for the sampled portion of
the middle Eocene averages 25 meters per million years,
decreasing upwards. Accumulation continued into the earlylate Eocene with an increase in the relative proportion of
the biogenic (mainly nannofossils) component of thesediment as represented by Unit 4. The provenance of theterrigenous detritus is probably a terrain of sedimentary or
low-grade metamorphic rocks with some volcanics. The
mineral assemblage includes quartz, muscovite, chlorite,
and plagioclase (andesine and albite). The detritus could
have been derived from either the southeastern PapuaLouisiade Archipelago region or from Queensland. The
latter seems the more likely since the sediments in thelower part of Hole 209 (mid Eocene) are glauconitic as is
the lower part of Unit 4 and also contain a significant
terrigenous component similar to that in Unit 5. Further, it
is suggested by Davies and Smith (1971) that metamorphism of the Mesozoic sialic rocks forming the core of
the southeastern Papua-Louisiade region took place in the
Eocene and that emergence of the metamorphics did nottake place until late Oligocene to early Miocene. No
turbidites have been recognized in Units 4 or 5. If they
were present they must have been thin and subsequently
have been destroyed by bioturbation.
Late Eocene-Early Oligocene
An angular unconformity represents most of late Eocene
and early Oligocene time during which the older sediment(Units 4 and 5) was folded. Folding may be related tocontinued tectonism in the Owen Stanley Range in eastern
Papua. Tectonism also took place at about this time in New
Caledonia and possibly the Solomon Islands. In addition,
slumped Eocene cherts occur near Port Moresby, Territoryof Papua and New Guinea.
Early-Middle Oligocene

Deposition of nannofossil ooze at oceanic depths near
the carbonate compensation level is represented by Unit 3.

376

Early-Middle Miocene
Deepening of the Coral Sea Basin and/or raising of the
carbonate compensation depth resulted in the slow
accumulation of abyssal clay at about 4 meters per million
years as represented by Unit 2. Although quartz, muscovite,
and chlorite are significant components in both this and the
Eocene section, the terrigenous detritus in these Miocene
beds differs somewhat from that in the Eocene section inthat potash feldspar is present and Plagioclase (andesine) is
more abundant. These compositional changes may reflect asource change to the Papuan region. This view is supported
by evidence of subsidence at Site 209 on the edge of the
Queensland Plateau and the deposition at that site of
predominantly biogenic sediments in the early to middle
Miocene. Wherever the source of the terrigenous debris, its
volume is insignificant compared to the terrigenous
component of the overlying Unit 1.
Late Miocene-Late Pleistocene
Accumulation of graded cycles of silt and clay via
turbidity currents took place in the early late Miocene tothe late Pleistocene as represented by most of Unit 1. The
largely terrigenous component of these turbidites probably
was derived from New Guinea based on mineralogy and on
the present bathymetry of the Coral Sea Basin (Winterer
and Galehouse, 1968). At the present time turbidity
currents enter the basin via the Moresby Submarine
Canyon. Although the beginning of turbidite deposition in
the Coral Sea Basin began in early late Miocene time,
deposition of similar types of sediment in the Aure Troughin New Guinea (approximately 30,000 feet of sediment ofearly Miocene to late Pleistocene age) began very early in
the Miocene with the sediment derived mainly from theOwen Stanley Range (Rickwood, 1968). The Aure Troughand the Coral Sea Basin may have been part of the samebasin in the Miocene with the Aure Trough acting as asediment trap for much of the detritus. Folding and upliftof the Aure Trough and many other areas of New Guinea
from the beginning of the Pliocene onwards (Rickwood,1968) provided additional source areas which accelerated
the rate of detrital input into the Coral Sea Basin. As
mentioned previously, the upper two-thirds of Unit 1
accumulated at a rate more than twice that of the lower
third.
Because there is no evidence indicating a shallowing of
the basin, the presence of considerable amounts ofnannofossil ooze intercalated with the graded cycles of silt
and clay indicates either a change in the compensation
depth compared to conditions prevailing during theaccumulation of Unit 2 or emplacement of the biogenic
interbeds by turbidity currents. If, as previously indicated,some of the biogenic interbeds in Unit 1 are turbidites,
turbidity currents may have been carrying debris into theCoral Sea Basin from more than one direction. In recent
times the elastics were probably derived from the northwest
via Moresby Submarine Canyon and the biogenics from thewest and southwest via Bligh Canyon (for details ofbathymetry, see Winterer, 1970). Earlier in the history of
deformation of Unit 1, terrigenous debris was probably
funneled through the Aure Trough, and the biogenic

SITE 210

interbeds were derived from the Omatai Trough, Fly River
Delta, Great Barrier Reef, and/or Queensland Plateau
regions.

BIOSTRATIGRAPHY
GeneralThe microfossils recovered from the 50 cores representing 711 meters of semi-continuously cored sediments
indicate the presence of an incomplete late early Eocene tolate Pleistocene sequence. Foraminiferal and calcareous
nannofossil assemblages enable the distinction of four
biostratigraphic units as follows: (1) Pleistocene to late
Miocene (210-1-1 to 210-30-2); (2) Mid Miocene to early
Miocene (210-31-1 to 210-33-5); (3) Mid Oligocene to lateearly Oligocene (210-33-5 to 210-34, CC);-Disconformity-(4) Early late Eocene to late early Eocene (210-35-2 to
210-50, CC).
1) The Pleistocene to late Miocene contains abundant tocommon, and well to moderately preserved foraminifera
and calcareous nannofossils. Authochthonous and reworked
assemblages (not older than Eocene) are present in varying
amounts in many cores. Autochthonous taxa are made up
primarily of tropical forms. Dissolution phenomena
observed in foraminifera indicate deposition close to oreven below the calcium carbonate compensation depth. The
preservation of tests was probably enhanced by rapid
sedimentation of the graded beds that prevented further
dissolution.
2) The mid Miocene to early Miocene sediments largely
lack microfossils, but small poorly preserved foraminiferaland nannofloral assemblages occur at several very thin andwidely separated horizons. The nannofossils at the base of
the interval are strongly corroded, thus suggesting that allof the interval was deposited below calcium carbonate
compensation depth.
3) The mid Oligocene and late early Oligocene
sediments contain foraminifera and nannofossils that arepoorly preserved as a result of dissolution effects. Thissuggests deposition close to the calcium carbonate
compensation level.
As in Sites 206 through 209, a disconformity separates
the Oligocene sediments from those of Eocene age. At thissite the latest Eocene and earliest Oligocene is contained
within the unconformity.
4) The early late Eocene to late early Eocene sediments
contain abundant but poorly preserved foraminifera andnannofossils, and at the upper part (210-35, CC to 210-40,
CC) a rare and porrly preserved radiolarian fauna. No
evidence of appreciable dissolution of the calcareous
microfossils was noted, suggesting that deposition wasabove the calcium carbonate compensation depth. Eocene
microfossils are represented by both tropical and temperate
forms, which is surprising for the present-day latitudinal
position of the site.
Foraminifera

Planktonic foraminifera in core-catcher materials from
Site 210 indicate the presence of an incomplete late early
Eocene to late Pleistocene sequence. Foraminiferal

assemblages and characteristics enable division into three
distinct biostratigraphic units as follows: (1) Pleistocene tolate Miocene (Cores 1 to 29) assemblages containing both
deep-water (lower bathyal-abyssal) benthonic foraminiferal
faunas and unreworked planktonic foraminiferal faunas, inaddition to reworked shallow-water (neritic-upper bathyal)benthonic foraminiferal faunas and reworked planktonic
foraminiferal faunas; (2) An essentially barren interval
between Cores 30 and Section 33-1; and (3) Oligocene toearly middle or late early Eocene foraminiferal faunas(Cores 33 to 50) that show little or no evidence ofreworking and which contain only relatively few benthonicforms.
Planktonic foraminifera indicate the presence of an
unconformity between 210-33, CC and 210-35, CCrepresenting at least the late Eocene (calcareous nannofossils show that part of the early Oligocene is also represented
within the unconformity between 2210-34, CC and 210-35,
CC). Otherwise, the foraminiferal sequence appears to berelatively continuous, although greatly complicated bystrong reworking in the Neogene, by strong dissolution
throughout much of the sequence, and by poorly preserved(often recrystallized) and sparse faunas, especially within
the Paleogene.
Middle Miocene to late Pleistocene faunas are made up
exclusively of tropical forms. Core-catcher samples
examined can be readily placed into three categories asfollows:
1. Well-sorted foraminiferal assemblages of small individuals that exclusively contain neritic and upper bathyalbenthonic foraminifera such as Quinqueloculina, Elphidium, discorbids, Nonionella, and costate uvigerinids.
Planktonic foraminiferal faunas are mostly composed ofwell-preserved (often delicate) small juveniles. Somesamples also contain reworked planktonic foraminifera as
old as the Eocene. This category is often associated withconspicuous plant debris and abundant mica, and isunquestionably almost entirely of reworked ("allochthonous") origin.
2. Foraminiferal assemblages containing various sizedindividuals that include: (a) unreworked planktonic foraminiferal assemblages made up primarily of solution-resistantforms such as Sphaeroidinella and Globigerina nepenthes
and which also are commonly fragmented as a result of
dissolution; and (b) deep-water (lower bathyal-abyssal)
benthonic foraminiferal faunas such as Melonis pompilioides, Pyrgo depressa, Globocassidulina, Eggerella, Pullenia

bulloides, and Pleurostomella. These faunas are unquestionably in place ("autochthonous") reflecting conditions
within the sedimentary basin itself.
The high degree of dissolution of these faunas indicatesdeposition close to or below the calcium carbonate
compensation depth. Preservation of faunas well below thislevel is possible because deposition of graded beds inrelatively rapid succession prevents further dissolution.
3. Mixtures of the above two categories.
The Pliocene-Pleistocene boundary is marked in Site 210
by the first appearance of G. truncatulinoides in succession
from G. tosaensis between 210-11, CC and 210-12, CC. The
Miocene-Pliocene boundary occurs between Cores 24 and
25.

377

SITE 210

Foraminiferal assemblages of early Miocene age have notbeen identified at this site, but according to thenannofossils, sediments of this age are represented within
the foraminiferal barren interval occurring between Core 30
and Section 33-1.
Paleogene planktonic foraminiferal faunas are represented by both tropical and temperate forms. Diversity issurprisingly low, considering the present-day latitudinal
position and probably represents evidence for northward
drift of the Coral Sea region since the Early Eocene.
Foraminifera are very rare or preservation poor over theinterval of the Oligocene-Miocene boundary as determinedby calcareous nannofossils. Oligocene faunas (210-33, CC)
are almost exclusively made up of Catapsydrax dissimilis.
Preservation is poor, largely as a result of dissolution
effects. This suggests deposition close to the calcium
carbonate compensation level.
Late early Eocene to middle Eocene sediments containabundant, although poorly to moderately preserved
planktonic foraminiferal faunas of relatively low diversity.
Poor preservation is largely due to recyrstallization anddistortion of specimens. No evidence of dissolution exists,suggesting deposition above the calcium carbonate compensation depth. A distinct preservation change, however,occurs within the Eocene assemblages between 210-36-2,
68-70 cm and 210-36-3, 103-105 cm. Above this level,
preservation is particularly poor while faunas below thislevel are moderately well preserved.
The boundary between early and middle Eocene
sediments is marked by the last appearance of Globorotalia
crater between Cores 41 and 42.
In summary, the middle Miocene to Pleistocene
foraminiferal sequence indicates much reworking ofshallow-water faunas to depths close to or deeper than the
calcium carbonate compensation depth. The Oligocene andEocene faunas contain no evidence of significant reworking.
Oligocene faunas reflect deposition close to the calcium
carbonate compensation depth, whereas Eocene faunas
were deposited above this depth.
Calcareous Nannofossils

Nannofloras extracted from Site 210 samples, which
represent 711 meters of semicontinuously cored sediment,
indicate the presence of an incomplete late early Eocene toPleistocene sequence at this site. The assemblages obtained,
together with an intervening essentially barren interval,
indicate the following age groupings which are arranged in
downhole order:
1) Pleistocene to early late Miocene (210-1-1, 10 cm to210-30-2,41 cm) lithologic Unit 1.
2) Mid Miocene to early Miocene (210-31-1, 36 cm to210-33-5, 51 cm) lithologic Unit 2 ("barren").
3) Mid Oligocene to late early Oligocene (210-33-5, 82
cm to 210-34, CC) lithologic Unit 3.
4) Early late Eocene to late early Eocene (210-35-2, 82
cm to 210-50, CC) lithologic Units 4 and 5.
As judged by the calcareous nannofossil content andpreservation, the whole of this sequence was deposited atabyssal depths close to the calcium carbonate compensation
depth; the nannofossil fraction having come from a378

warm-water environment which was largely, but not
exclusively (especially in Unit 1), of an oceanic nature.
As in the sequences at Sites 206 to 209, an
unconformity involving most of the Late Eocene plus theearliest Oligocene is present.
The deposition rates for this sequence, as based entirelyon the calcareous nannofossil age determinations, areshown in Table 3.
TABLE 3
Deposition Rates for Site 210
Interval

Meters per Million Years

Zone NN21 (Pleistocene)
Pleistocene (in toto)
Late Pliocene
Early Pliocene
Late Miocene
Early and,Mid Miocene
Oligocene
Late Eocene
Mid Eocene

49
70
75

Site 210

ca60
ca24
7

not determinable
not determinable
25 (upward
decreasing)
13

The continuing high deposition rate during Zone NN21,
the last 250,000 years, can be used to give a calculated
average periodicity of emplacement for the youngest Unit 1
clastic graded cycles of one per 4,800 years. If theintervening nannofossil ooze beds are included, and someundoubtedly should be (see below), the periodicity rate is
reduced to one per 3,500 years.
The samples taken for nannofossils from the interval
210-1-1, 10 cm to 210-12-3, 13 cm (Pleistocene) are
distincly biased in favor of the nannofossil ooze interbeds
and the lightest colored tops of the clastic graded cycles.
Usually these lithologies contain abundant, moderately wellpreserved, diverse and common, moderately well preserved,
low diversity, nannofloras, respectively. A few samples werealso taken from the darker colored clastic lithologies, butthese either lacked nannofossils or contained very rare to
few poorly preserved (corroded) very low diversity (mostly
either Gephyrocapsa or Pseudoemiliania) nannofloras.
Taxa present in this interval and considered to be moreor less penecontemporaneous with deposition include
Ceratolithus cristatus, Cyclococcolithina leptopora, C.
macintyrei (unreworked top about 210-104, (88 cm),
Cyclolithella annula, "Doscoaster"perpelxus, Discosphaera
tubifer, Emiliania huxleyi (210-1-1, 35 cm; 210-1-1, 130
cm; 210-1, CC; and 210-2-2, 90 cm, Gephyrocapsa
caribbeanica s.l. (base at 210-11, CC common and usuallywith cross-bar), G. oceanica (base at 210-7, CC usually withcross-bar), G. sp. (210-8, CC to 210-12-3, 13 cm range),
Helicopontosphaera kamptneri et aff, Pontosphaera discopora et aff, P. japonica, P. scuttelum, Pseudoemiliania
lacunosa (unreworked top about 210-5, CC), Rhabdosphaera claviger, Sycphosphaera spp., Syracosphaera
histrica, Thoracosphaera heimii, and T. perforata. Also
observed throughout were globostellate ascidian sclerites
and "planktonic" microforaminifera—both having theirhighest occurrences in 210-1-1, 130 cm and their greatest
abundance in nannofossil ooze from 210-5, CC. In many

SITE 210

samples a distinct association between the relative
frequencies of intact ascidian sclerites, microforaminifera,
Scyphosphaera lopodoliths, Thorasocphaera nannospheres
and, less obviously, large Pontosphaera discoliths wasnoted. This association of large nannofossils, which isparticularly conspicuous in nannofossil ooze samples
210-1-1, 130 cm; 210-3-3, 50 cm; 210-5, CC; 210-6-4, 80
cm; 210-94 98 cm; and 210-10-4, 88 cm could be due tosize sorting during deposition.
Other taxa observed in this interval and attributed toreworking include Ceratolithus rugosus (reworked in part?),
Chiasmolithus grandis, C. solitus, Coccolithus eopelagicus,
C. pelagicus, Cyclicargolithus floridanus, Cyclococcolithina
formosa, C. macintyrei (reworked in part), Discoasterasymmetricus, D. barbadiensis, D. brouweri, D. deflandrei,
D. pentaradiatus, D. surculus, D. variabilis, Helicopontosphaera parallela, Micrantholithus basquensisl, Pseudoemiliania lacunosa (reworked in part), Reticulofenestra
bisecta, R. placomorpha, R. pseudoumbilica, Spenolithus
abies, S. cf. distentus, S. moriformis, S. neoabies,
Zygolithus dubius, and Zygrhablithus bijugatus. Almost all
samples were found to contain at least a few specimens
attributable to reworking from, as the above list indicates,
mid Eocene and younger sediments. In most of these cases
the source appears to be primarily, but not exclusively, of
Pliocene age. In one sample, 210-1, CC, such reworking
represents a substantial part of the flora. However, by way
of contrast, Samples 210-1-1, 130 cm; 210-8, CC, and210-104, 88 cm contain massive reworking from sediments
mainly of early Miocene age. Clearly more than one sourceof reworking was being actively eroded.
A lithologic sequence such as occurs in this and theunderlying Plicoene and late Miocene intervals is usuallyconsidered to result from episodic influxes of elastics with
the intervening pauses allowing normal pelagic deposition
to occur to a greater or lesser extent. However, in thisparticular case there are good reasons for considering asignificant and perhaps major part of the biogenic
interbeds, which represent about 20% of this interval, as
having been deposited by the same method as the elastics.
The grounds for this conclusion are that: (1) a very low
accumulation rate for strictly pelagic sedimentation is
expectable at the present 4650 meters depth of Site 210;(2) the calcareous nannofossils in the biogenic interbeds are
surprisingly well preserved (e.g., uncorroded Scyphosphaera, Rhabdosphaera, Syracosphaera, perforate Pontosphaera etc.) whereas those in the upper parts of the moststrongly clastic graded cycles are strongly corroded;(3) the
consistent presence of reworking, occasionally massive,
regardless of lithology indicates redeposition as probably
does the occurrence in the biogenic interbeds of apparent
size sorting (see above); and (4) the probably shallow
sublittoral origin of the ascidian sclerites present, often
conspicuously, in all but the most strongly clastic
lithologies.
From the above, it must be obvious that accurate age
and zone assignments in this and the similar underlying
intervals are difficult to achieve. Clearly the observed basesof abundant taxa are the most reliable criteria to use but
even these are at best going to be close approximations dueto the general prevalence of more or less unfavorable facies.

Equally clearly the tops of taxa known to be usefulelsewhere are not going to be very reliable because of the
problem of reworking. For example, Sample 210-1-1, 35
cm contains the highest occurrences of the taxa defining
the tops of the NN15, NN16, NN17, NN18, and NN19
zones of Martini (1971) plus the highest occurrence of thestill living index of his youngest, NN21 zone. However,despite this it is often possible, as has been done for the
purposes of this report, to determine subjectively the"unreworked top" of a taxon based on an observed upwardchange in its consistency of occurrence and frequency.
Accordingly the following approximate correlations are
made, in downhole order, for this interval: 210-1-1,10 cm
to 210-2-2, 90 cm; Pleistocene 3/3, Emilinia huxleyi(NN21) Zone of Martini (1971); probably reliable; 210-2-3,
120 cm to 2104, CC, Pleistocene 2/3, Gephyrocapsa
oceanica (NN20) Zone of Martini (1971), low reliability(gap zone); 210-5, CC to 210-12-13, 13 cm, Pleistocene
1/3, Pseudoemiliania lacunosa (NN19) Zone of Martini(1971), probably moderately reliable.
The Pliocene to late Miocene nannofloras are essentiallysimilar to those of the overlying Pleistocene (q.v.) exceptthat a downward decrease in the quality of preservation andamount of reworking is evident. Despite this, theassemblages can, with relative ease, be correlated with thezonal scheme of Martini (1971) as indicated on the barrelsummary sheets. The Plio-Pleistocene and early-late
Pliocene boundaries sensu calcareous nannofossils are easily
recognized, being based on the last continuous appearancesof abundant unbattered Discoaster brouweri and Reticulofenestra pseudoumbilica, respectively. The same is not,however, true of the Miocene-Pliocene boundary nor of theage of the base of this interval, neither of which can belocated accurately.
The mid Miocene and early Miocene nannofloras are
represented by very small, poorly preserved assemblages
which occur in thin horizons widely separated by barren
clays. This information coupled with the essentiallyreworked nature of the calcareous nannofossils at 210-33-1,
31 cm and the highly corroded nature of the 210-33-5, 52
cm assemblage strongly suggest that deposition at this site
was below the calcium carbonate compensation depth
throughout early and mid Miocene. The coincidence of an
abrupt change in both facies and flora at the base of thisinterval suggests it represents either a highly condensed
sequence or an unconformity.
The mid Oligocene to late early Oligocene contains
abundant but poorly preserved and not very diverse
nannofloras which approximately correlate with the zonal
schemes of both Edwards (1971) and Martini (1971).
Spenoliths other than those of the S. moriformis type arevery rare throughout.
The early late Eocene to late early Eocene nannofloras
aç> abundant and diverse but poorly preserved. In
containing taxa such as Chiasmolithus gigas, Spenolithus
furcatolithoides, and Triquetrorhabdulus inversus theseassemblages clearly have been deposited from a warmer (?
tropical) climate than that indicated by age-equivalent
floras from New Zealand, some 30° to the south. Despite
this, both readily fit into the zonal scheme of Edwards(1971)—a rather surprising result.

379

SITE 210
Radiolaria

The single radiolarian occurrence at this site wasrecorded in Samples 210-35, CC to 210-40, CC in thestratigraphic interval between middle middle Eocene andearly middle Eocene. Radiolarians are rare and poorly
preserved.
Unlike the middle Eocene radiolarians encountered at
Sites 206 to 208, which were of subtropical and temperate
type, and which, due to the absence of the index species,
could not be assigned to the zonation recently establishedby Riedel and Sanfilippo (1970) for tropical regions, theassemblages encountered at this site are similar in species
composition to those commonly encountered in thetropics. The zonation established for tropical radiolarians iswholly applicable to them.
Sample 210-35, CC seems to belong to Podocyrtis mitra
Zone (middle middle Eocene). The following species havebeen recognized: Podcyrtis mitra, Lychnocanium helium,
L. splendens, Calocyclas turris, Theocampe mongolfieri,
Thyrsocyrtis triacantha, Phormocyrtis striata, Lithochytris
vespertilo.
In Sample 210-36, CC radiolarians are so poorly
preserved that they are impossible to identify, even at thegeneric level. The 210-37, CC to 210-39, CC samples are in
the Thyrsocyrtis triacantha Zone. The assemblage iscomposed of Thyrsocyrtis triacantha, T. hirsuta, Phormocyrtis striata, Theocotyle ficus, Podocyrtis aphorma, P.
papalis, Calocyclas hispida, Lithochytris archaea, etc.
In 210-40, CC only one species, Theocampe sp., wasencountered.
PHYSICAL PROPERTIES
Bulk Density

As with earlier sites, GRAPE determinations of bulk
density are plotted in the hole summaries. It must be
realized that the upper part of the sequence cored at Site
210, consisting of graded beds of silt and silty clay
interbedded with clays and oozes, is considerably more
complex than the other sequences drilled on Leg 21.
Consequently, we cannot attach any particular significanceto discussions of the average density. Despite thislimitation, however, the effect of compaction can clearly beseen between 50 and 100 meters below the sea bed, where
the density rises markedly from 1.49 to 1.65 gm/cc into therange 1.7 to 1.8 gm/cc. Below this depth there is a steadyincrease in density downwards to the bottom of lithologic
Unit 1 (430 m p = 1.94 gm/cc). Densities throughout thisunit are generally a little lower than densities at comparable
subbottom depths in the ooze sequences. This may simply
reflect compositional differences. In detail, the GRAPE
curves for this upper part of the sequence show theindividual graded beds very clearly. In general, the upper
part of each bed is noticeably denser than the basal part.
This presumably reflects the increased porosity of thelower, coarser silt and fine sand layers.
In Cores 31 and 32 (lithologic Unit 2) the density drops
into the range 1.69 to 1.81 gm/cc. These cores are almost
entirely silty clay.
Below Core 32 (lithologic Units 3-5) the density rises
abruptly to values greater than 2.0 gm/cc, as a consequence380of the vastly increased carbonate content, and becomessurprisingly variable. Since this part of the sequence islithified, the variation in density presumably reflects bothchanges in cementation and changes in composition. This isborne out by the strong correlation between variation indensity with subbottom depth and the variation incarbonate content with subbottom depth (see Lithology
section). High density is correlated with high carbonate
content and vice versa.
Sonic Velocity
Above Core 23 the velocity is virtually constant in therange 1.49 to 1.65 km/sec. This is generally lower than thevelocity in comparable ooze sections.
Below Core 23 the velocity becomes variable, but
generally increases to rise abruptly to 2.0 km/sec with anincrease in density at the top of lithologic Unit 3 (Core 33).
In the lower oozes and chalks the velocity is in the range
2.07 to 3.03 km/sec and is very variable, as might be
expected from the behavior of the density curve. A velocity
maximum of 3.03 km/sec is reached in Core 36 below
which the velocity generally but irregularly decreases. This
corresponds to a general decrease in the amount ofcarbonate material, with the attendant decreases in
hardness and density. However, unlike the density curve,
there is no obvious correlation in detail between the
carbonate curve and the velocity curve.
Thermal Conductivity and Heat Flow

Thermal conductivity was measured by the needle probe
method on cores recovered from this site at subbottom
depths up to 520 meters (Core 33). Below about 275
meters (Core 20), the cores were sufficiently indurated thata special long drill was used to create the hole required forthe needle probe. In a few instances, this resulted in core
fracture, which may affect the measurements. For the mostpart, no disturbance was apparent and reasonable values
were obtained.
Values range from 2.1 to 3.6 m cal/°C cm sec (TCU),
uncorrected for sea floor ambient pressure and temperature, there is substantial variation between cores and evenbetween sections of the same core, which is most readily
explained by the turbidite stratification. The variations
probably reflect the proportions of carbonate (highconductivity) versus that of clay (low conductivity) in thesesediments. The values show a general increase with depth,
except below 450 meters where the reverse seems to betrue. It is of interest to note that the values measured in the
more indurated sediments below 250 meters depth are only
slightly higher (10%) than most of those measured between
70 and 170 meters depth, suggesting that the water content
of these sediments has not changed markedly withlithification.
A downhole temperature measurement at 54 meters gave
a value of 7.16 ± 0.1°C. Combining this with abottom-water temperature of 1.93°C, as measured within
the drill pipe on the same lowering, results in a gradient of
0.097°C/m to 54 meters depth. The average thermal
conductivity to this depth of 2.4 TCU gives a heat flow of
2.3µ cal/cm2 sec, nearly twice the oceanic average and thehighest measured on Leg 21.

SITE 210
SUMMARY AND CONCLUSIONS

Site 210 was drilled near the center of the Coral Sea
abyssal plain above a section of relatively high and rough"basement" relief. The seismic profiles of the site survey
and the site approach show an alternation of reflective andnonreflective zones in the upper 0.65 sec, suggesting
stratified and homogeneous sediments resting on a roughbasement. However, drilling penetrated five lithostratigraphic units, ranging in age from late early Eocene to late
Pleistocene, and demonstrated that the alternation ofpatterns in the profiles is a product of turbidite spacings,
calcareous content of the sediment, and lithification. The
rough basement reflector under much of the basin is either
the upper surface of a chalk horizon, or a high to low
velocity transition downhole in the lowest clay/chalk unit.
Unit 5, from 554.4 to 711 meters, is a clay nannofossil
chalk of late early to middle Eocene age. Sonic velocities
within this unit decrease irregularly in response to thevarying clay/calcite ratio, and produce Reflector 4—thedeepest coherent reflector seen in the seismic profiles.
Depth to true basement is uncertain, but is probably over
1 km subbottom based on faint indications in the sonobuoy
profile. Unit 4, from 540 to 554.4 meters, is middle toearly late Eocene in age and is a clay-bearing calcareous
nannofossil chalk with minor chert nodules. Unit 3, from521.6 to 540 meters, is a clay-rich chalk of late early to
middle Oligocene age. Unit 2, from 470 to 521.6 meters, isa largely unfossiliferous abyssal clay of early to middle
Miocene age. Reflector 3 corresponds to the boundary
between Units 2 and 3. Unit 1, from 0 to 470 meters, iscomposed of approximately 1900 turbidite layers of silt
and clay with intercalated layers of nannofossil ooze which
may also have largely been emplaced by turbidity currents.
Rare nonturbidite silty sand layers also occur. This unit
ranges from early late Miocene to late Pleistocene in age.
The increase in thickness of the nannofossil layers in thelower third of the unit gives rise to Reflector 2.
The lithostratigraphic and biostratigraphic records andthe seismic profiles permit an interpretation of the basin's
history. During early to late Eocene time clay, foraminifera,
and nannofossils accumulated as a pelagic blanket at depths
generally above the lysocline. Chert nodules appear in thelater portion of this time interval and may be related toevents producing the Eocene/Oligocene unconformity. At
Site 210 the regional unconformity represents most of late
Eocene and early Oligocene time. Dips in the beds of Units
4 and 5, the rough surface of Reflector 4, and the draped
appearance of Reflector 3 suggest that disturbance of thebasin floor, possibly in the form of folding, took place
during this time gap. In late early to middle Oligocene time
sediments were deposited below the lysocline and near the
carbonate compensation depth. The abyssal clays of Unit 2
indicate either deepening of the basin below thecompensation depth and/or raising of the carbonate
compensation depth itself during early and middle Miocene
time. During early late Miocene to Pleistocene time,
deposition of Unit 1 took place.
Basin morphology and the mineralogy of the detrital
sediment in the turbidite sequences of silt and clay (Unit 1)
indicate New Guinea as the major source of this detrital

sediment. Detrital material in Units 4 and 5 may have been
derived from Queensland and show affinities to sedimentsin the lower portion of Site 209 (glauconite and terrigenous
components).
REFERENCES
Davies, H. L. and Smith, I. E., 1971. Geology of eastern
Papua: Geol. Soc. Am. Bull., 82, p. 3299-3312.
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.
Gardner, J. V., 1970. Submarine geology of the Western
Coral Sea: Geol. Soc. Am. Bull., v. 81, p. 2599.
Martini, E., 1971. Standard Tertiary and Quaternary calcareous nannoplankton zonation: Planktonic Conf., 2ndRome 1970, Proc, p. 739-785.
Rickwood, F. K., 1968. The geology of western Papua: J.
Aust. Petrol. Expl. Assoc, v. 8, p. 51-61.
Riedel, W. R. and Sanfilippo, A., 1970. Radiolaria, Leg 4
Deep Sea Drilling Project. In Bader, R. G. et al., Initial
Reports of the Deep Sea Drilling Project, Volume IV.
Washington (U. S. Government Printing Office), p. 503576.
Winterer, E. L., 1970. Submarine valley streams around theCoral Sea Basin (Australia): Mar. Geol., v. 8, p. 229-244.
Winterer, E. L. and Galehouse, J. S., 1968. Sedimentationin the Coral Sea Basin (abstract): Geol. Soc. Aust.,
Progr. Ann. Meeting, Canberra, 1968, p. 13.

NOTE CONCERNING THE APPENDICESThe appendices consist of tables of shore laboratory determinations of grain size, carbon content, and mineralogjcal 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 results of
shipboard examination of smear slides of each lithology. In order tomake the lithologic descriptions more complete we have also included many of the shore laboratory results. These are identified bybeing placed in square brackets.

APPENDIX A
Grain Size Determinations, Site 210

Core, Section,
Top of
Interval
(cm)

Depth
(cm)

Sand

Silt

Clay

(%)

(%)

(%)

Classification

12-4,101.0
12-4,108.0
124,117.0
13-2,685.0
13-2,82.0
13-2,90.0
32-6,24.0

127.5
127.6
127.7
148.4
142.3
142.4
503.7

0.1
0.0
0.1
0.0

20.4
54.6
71.3
12.7
28.2
60.0
19.5

79.5
45.4
28.6
87.3
71.7
39.3
80.2

Clay
Clayey silt
Clayey silt
Clay
Silty clay
Clayey silt
Clay

0.0
0.7
0.2

381

SITE 210

APPENDIX B
Carbon-Carbonate Determinations, Site 210
Core, Section,
Top of
Interval(cm)
1-2,99.0
1-2,112.0
1-2,105.0
1-2,117.0
1-3,50.0
1-3,55.0
1-3,70.0
1-3,117.0
1-3,130.0
1-3,137.0
2-6,25.0
2-6,46.0
3-3,19.0
3-3,24.0
3-4,66.0
10-4,88.0
10-4,97.0
10-4,107.0
10^,116.0
11-2,32.0
11-2,42.0
11-2,49.0
11-2,52.0
11-2,55.0
11-2,60.0
11-2,67.0
14-2,73.0
14-2,82.0
14-2,88.0
14-2,95.0
21-1,72.0
24-6,131.0
32-6,24.0
34-1,76.0
34-4,123.0
35-4,118.0
36-1,72.0
36-4,36.0
37-3,100.0
38-2,73.0
39-2,38.0
40-3,38.0
41-2,59.0
42-1,52.0
43-4,87.0
44-2,95.0
45-2,103.0
46-4,61.0
47-3,26.0
48-2,51.0
49-2,79.0
50-4,127.0

382

Depth
in HoleCarbonTotal

Organic
Carbon

CaCO,

(m)

(%)

(%)

(%)

2.5
2.6
2.5
2.7
3.5

1.9
1.9
1.2
1.6
0.4

0.4
1.3
0.9
0.0
0.3

13
5
3
14
1

3.5
3.7
4.2
4.3
4.4

0.4
1.2
1.4
0.9
1.6

0.3
0.7
0.8
0.7
1.2

1
4
5
2
4

16.8
17.0
21.2
21.2
23.2
86.4
86.5
86.6
86.7
104.8
104.9
105.0
105.0
105.1
105.1
105.2
161.2
161.3
161.4
161.4
291.7
355.8
503.7
533.8
538.7
547.7
551.7
555.9
564.0
571.2
579.9
590.4
598.1
605.5
619.4
625.5
634.5
653.1
668.3
680.0
694.3
707.8

1.8
1.4
1.9
4.1
7.1

0.7
0.3
1.3
0.2
0.7

9
9
5
32
53

9.8

0.1
0.1
0.1
0.1
0.4

81
84
0
91
63

1.3

0.3
0.2
0.2
0.6
0.3

70
70
4
8
9

1.2
4.8
0.4
0.4
1.0

0.2
0.2
0.3
0.3
0.5

8
38
1
1
4

8.8
3.0
0.2

0.1
0.2
0.1
0.0
0.0

72
24
1
87
90

9.2
6.5
8.1
7.4

0.0
0.1
0.1
0.1
0.1

85
76
53
67
60

7.9
6.1
7.0
5.9
7.2

0.1
0.2
0.1
0.1
0.1

65
50
58
48
59

5.6
5.9
4.7
5.4

0.1
0.2
0.1
0.1
0.1

46
43
48
38
44

5.2
3.7

0.1
0.1

43
30

10.1
0.0

11.1
7.9
8.7
8.6
0.6
1.6

10.5
10.8
10.3

5.3

APPENDIX C
X-ray Mineralogy Determinations, Site 210
Core

Cored
Interval
Below Sea
Floor (m)Sample Depth
Below Sea
Floor
(m)

Arag.

Qua

Clin.

Phil.

Pyri.

Amph.

1.0

1.6
2.4
2.9
1.6
3.1

U-l d

IM

Bulk Sample

0.3
4.7
8.8
9.4
12.8
16.8
17.0
21.1
23.2
6
8
9
10

12
20
21

45-54
63-72
72-81
81-90

122-131272-281291-300

328-33724

347-35625

365-374

28
29
30
31
32
34
35
36

00

37
38
39
40
41
42
43
44
45
46
47
48
49
50

421-430
440-449459-468
477-486496-505
533-542542-551551-560
560-569569-578578-587587-596596-605605-614614-623623-632632-641648-657665-674678-687692-701702-711

69.7
70.2
86.0
86.6
104.7
105.1
126.1
273.3
291.7
293.0
311.4
315.1
315.3
315.5
329.3
334.0
349.6
355.8
365.8
368.2
370.6
407.1
411.9
429.5
443.9
462.8
480.1
503.7
533.7
547.7
551.7
555.8
564.0
571.3
579.8
590.4
597.5
605.6
619.4
625.5
634.5
653.1
668.3
680.0
694.3
707.8

79.9
80.8
79.9
74.9
73.3
81.5
83.9

68.7
70.0
68.7
60.8
58.3
71.1
74.9

79.7
70.1

68.3
53.3

77.7

65.2
71.0
46.9
33.1
69.3
36.6
48.2
61.4
77.3
68.8
38.1
53.3
66.6
73.0
70.2
52.3
57.2
60.7
64.3
58.3
58.2
48.7
53.6
56.5
62.8
54.0
62.6
50.9
70.1
77.7

81.4
66.0
57.2
80.4
59.4
66.8
75.3
85.5
80.0
60.4
70.1
78.6
82.7
81.0
69.5
72.6
74.9
77.1
73.3
73.3
67.2
70.3
72.2
76.2

70.6
76.2
68.6
80.8
85.7

56.2
65.8
61.5
63.9

31.6
46.6
39.8
43.5

33.8
55.9
57.2
61.6
59.0
59.0
62.9

31.2
33.1
40.0
35.9
35.9
42.0

61.6
2.3
3.4

-

9.0
11.6
3.9
32.6

30.1

58.8

11.6

3.6
26.4
7.2
37.8
26.0
6.8

92.7
53.3
31.4
5.2
5.6
72.8
45.1
10.1
40.5
24.8
51.1
8.4
9.0
3.0
13.8

54.3
14.3
61.8
40.9
1.9
2.2
19.9

4.1

10.1
_

98.0
97.4
92.6
78.9
78.2
82.4
81.7
63.0
73.9
68.5
65.7
65.7
55.4
67.7
54.4
61.3
62.6
40.6

12.3
31.4
33.3
38.9
43.5
27.4
23.5
42.2
18.5

-

4.0

1.8
4.3
0.7
-

11.1
29.1
12.1
3.6
31.8
0.4
23.2
32.2
24.9
30.0
3.2
18.6
12.7
26.8
23.1
7.2
23.1
26.5
13.5
15.3
6.5
40.7
22.5
33.5
31.2
27.1
18.7
35.7
17.7
18.6

2.1
4.0
4.0
3.7
2.4
3.7
4.6
6.6
23.0
26.6
33.2
22.7
34.2
28.4
29.2
41.9

-

5.1
6.6
3.7
4.1
6.1
3.5
1.3
5.0
2.3
3.1

5.2
3.8
14.6

_
2.3
3.7
9.0
18.2
12.6
15.9
_

18.6
24.7
28.8
36.4
23.9
16.2
23.4
6.2
2.9
18.7
3.3
2.5
22.4
6.9
33.1
13.2
19.4
1.3
9.0
7.8
15.8
13.6
2!5
11.7
31.1
8.7
19.1
12.4
25.1
27.1
31.5
24.2
22.3
20.5
28.9
21.0
11.9

1.5
1.5
1.0
1.1
1.8
0.9

0.8
1.1
1.2
1.3

2.1
5.4
3.7

1.2
2.4
2.1
0.6
3.9
3.1

2.1
4.4
12.1
2.7
3.4
1.4
4.1
5.0
2.2
2.7

3.4

13.7
34.4
28.1
22.8
12.7
24.0
29.2
18.5
7.7
9.9
31.3
2.1
2.0
26.7
2.9
17.2
31.6
9.3
2.8
7.7
13.0
29.8
33.4
8.3
9.9
22.6
19.0
13.0
5.8
18.9
27.5
14.7
16.9
35.2
33.2
26.2
38.8
16.0

1.6
4.6
5.2
3.5
2.2
4.1
2.4
3.1
3.0
4.4
5.7
4.6
5.4
5.3
4.3
12.0

2.9
5.3
4.2
5.4
3.4
5.9
5.8
4.8
1.2
1.8
8.2
0.6
0.6
6.3

1.8
1.1
3.1
8.2
2.7
1.2
3.3

4.0
6.3
-

0.2
5.0
13.4

1.6
2.0
8.2
8.8
0.9

1.3
3.8
6.7
7.8
2.0

1.3
6.2
4.9
3.0
1.9
5.2
6.3
5.0
5.5
8.1
9.6
8.1
6.9
3.7

1.6
1.0
4.3
3.4
13.6

—
-

2.2
3.3
8.7
4.5
1.5
7.4
2.0
2.9
3.6
2.7
-

0.7
1.5
1.5
1.7
4.3

4.3
3.6
2.5
1.1
_

7.5
2.6

1.4
0.5

2.5

7.3
8.0

0.8

0.7

1.6
0.8

1.6
3.2
5.2
1.2
16.1
10.0
31.9

—
1.8
1J2

3.2
2.5
2.8
2.1
5.7
_

1.4
3.6

-

7.8
1.8

1.2
1.3

_

0.6
_

1.4
1.4
1.1
1.6

Trace
Trace
Trace
Trace
Trace
Trace
Trace
Trace
Trace

Trace
Trace
Trace

Apat.

APPENDIX C - Continued

00

Core

Cored
Interval
Below Sea
Floor (m)Sample Depth
Below Sea
Floor
(m)

Arag.

Quar.

Cris.

Plag.

Pyri.

Amph.

U-l

a

Apat.

2-20µ Fraction
0-9

HI)!
4.7
8.8

78.0
70.0
72.8

65.7
53.1
57.5

37.0
37.5
1.2

9.4
12.8
16.8
17.0

71.3
70.7
72.8
77.9

55.2
54.1
57.5
65.5

38.8
37.4
32.0
34.0

21.1
23.2

71.9
71.7

56.0
55.7

69.7
70.2

66.0
68.2

27.9
23.6
98.7

23.9
30.1

7.5
7.6

5.1
5.2
3.2

28.0
31.4
27.4
23.9

24.9
17.6
24.6
29.5

44.6
58.9

4.8

24.9
19.5

21.8
11.8

5.4
5.3
7.7
7.6
6.2
1.9

17.5

1.7

46.9
50.3

28.4
49.5

4.5
6.7

20.3
20.3

35.8
16.5

9.7
3.5

-

0.9
0.5
1.1
2.1
1.0

1.7
1.2
0.1
2.1
3.2
2.5
1.7
1.3
1.1
1.3

6
8

45-54
63-72

9

72-81
81-90

73.8

75.9

62.4

35.5

3.3

29.7

22.2

8.0

3.5
-

86.0

68.5

50.8

32.0

2.7

25.4

29.2

8.1

1.1

103-112

104.7
105.1

61.4
68.9

39.7
51.4

56.2
29.7

8.7
5.2

23.6
30.2

6.9
23.3

0.7

2.0
1.3

1.3
1.6
2.0
3.4

10
11
12
20
21

45.6

5.5

6.8

122-131

126.1

70.2

53.4

33.6

5.4

21.9

29.4

6.2

272-281291-300

273.3

67.3

48.9

28.5

6.6

19.6

35.4

9.5

291.7
293.0

73.0
67.6

57.8
49.4

37.8
25.6

11.4
8.1

24.9
22.(1

20.1
31.4

5.7
8,2

311.4
315.1
315.3
315.5

68.1
59.6
66.9
66.7

50.2
36.8
48.3
48.0

30.8
52.5
26.0
45.1

4.2
9.3
6.0
7.1

27.0
22.3
18.3
17.1

23.2
10.8
38.4
24.4

7.5
1.4
11.2
3.9

6.1
2.6

1.2
0.9

13.3
24.9

0.6
11.1

0.8
1.9

1.7
1.4

27.8
11.8
33.6
25.9

9.0

2.4

23

328-337

329.3
334.0

57.7
68.4

34.0
50.6

46.7
26.6

24

347-35625

365-374

349.6
355.8
368.2
370.6

68.2
67.3
62.9
63.5

50.3
48.9
42.0
43.0

27.1
16.3
31.7
26.2

27

403412

407.1
411.9

69.3

52.0
55.2

29.2
33.2

21.5
25.5

18.3
17.2

6.6

71.3

28
29

429.5

59.4

36.6

22.6

21.1

39.1

13.4

443.9

62.2

41.0

19.9

20.9

42.4

13.8

30

421-430
440-449459-468

462.8

58.0

34.3

25.3

23.3

36.2

13.8

31
32

477-486496-505

480.1

66.9

48.2

24.0

5.6

27.5

31.5

10.0

503.7

75.6

61.9

30.4

26.0

20.9

17.2

2.4

36

551-560

551.7
555.8

66.9

48.3
49.0

34.4

14.3

20.4

560-569578-587

12.4

28.7

37
39
40
41
42

564.0

587-596596-605605-614

590.4

43
44

614-623623-632632-641648-657665-674692-701702-711

619.4

45
46
47
49
5

579.8

597.5
605.6

625.5
634.5
653.1
668.3
694.3
707.8

67.3
66.7
83.4
79.1
77.4
76.1
62.4
60.4
57.7
63.1
57.0
58.2
51.5

47.9
74.1
67.4
64. S
62.6
41.2
38.1
34.0
42.3
32.8
34.7
24.2

28.2

24.8
34.1
5.7
4.4

3.0

2.6

24.5
18.9
21.7
29.2

5.2

8.0
11.9

0.6
-

2.2
-

16.4

21.7

50.5

8.5

12.5

0.8

16.0

47.4

6.5

15.0

1.0

26.9

39.5
27.9

0.8

9.1
3.8
3.9
4.3

α

2.5
2.0
1.2
3.1
2.4
1.5
1.4

30.9
25.6
25.1
0.8
_

4.2

8.5

16.2

4.3

8.3

23.1

65.3

6.7

6.4

18.6

63.1

6.8

5.0

21.5

71.1

5.1

4.9

16.8

1.1

66.0

6.4

5.8

18.3

1.0

2.6

68.2

11.7

15.7

2.9

1.5

84.7

10.5

3.0

1.9

68.4

10.4

4.1

7.5
4.4

32.2

1.5
1.2

0.03
4.7
8.8

82.4
81.1
80.6

72.6
70.5
69.7

14.5
13.6
13.3

9.4
12.8
16.8
17.0

79.1
81.0
80.3

67.3
70.4
69.2
74.3

12.6
11.7
16.0
17.4

2.5
1.7
1.8
1.6

5.0
8.1
8.3

2.3

1.0

<2µ Fraction

i

1.4
0.9
14.5
3.4
0.8

11.6
7.0

17.8

36.9

1.1

38.6

5.7
3.9
3.5

21.2
39.2
35.3

6.6
10.3
8.3

44.5
28.6
37.5

4.4
11.1
3.9
7.4

38.5
33.7
27.9

X.2
7.1
X.2
6.7

33.2
29.7
34.1
30.1

3
6
8

18-27
45-54
63-72

9
10
11

72-81
81-90
103-11212
20
21

122-131272-281291-300

22309-31823

328-33724

347-35625

365-37427

403-412

28
29
30
31
32
34
35
36

421-130
440-449459-i68
477-486496-505
533-542542-551551-560

37
38
39
40
41
42
43
44
45
46
47
48
49
50

560-569569-578578-587587-596596-605605-614614-623623-632632-641648-657665-674678-687692-701702-711

a

b

21.1
23.2
49.4
69.7
70.2
73.8
86.0
104.7
105.1
126.1
273.3
291.7
293.0
311.4
315.1
315.3
315.5
329.3
334.0
349.6
355.8
365.8
368.2
370.6
407.1
411.9
429.5
443.9
462.8
480.1
503.7
533.7
547.7
551.7
555.8
564.0
571.3
579.8
590.4
597.5
605.6
619.4
625.5
634.5
653.1
668.3
680.0
694.3
707.8

83.1
81.5
80.8
83.8
81.1
83.1
79.5
79.6
76.7
82.7
80.1
82.4
78.6
81.9
83.7
79.4
80.8
79.9
71.1
81.2
81.0
76.0
71.7
84.7
74.0
84.2
73.9
84.1
76.2
81.5
84.6
82.3
72.9
79.7
84.5
76.5
81.2
85.4
81.6
82.7
81.2
63.9
61.4
57.3
60.1
66.4
64.3
71.9
63.8

73.6
71.0
70.0
74.7
70.5
73.6
68.0
68.2
63.5
73.0
68.9
72.4
66.6
71.7
74.5
67.8
69.9
68.5
54.9
70.7
70.3
62.4
55.8
76.1
59.4
75.3
59.2
75.2
62.8
71.1
75.9
72.4
57.6
68.2
75.7
63.3
70.6
77.2
71.3
73.0
70.6
43.7
39.8
33.2
37.6
47.6
44.2
56.1
43.5

-

-

-

-

-

_

-

-

17.4
12.4
15.0
19.0
10.4
16.5
12.9
9.9
10.6
19.3
19.6
17.8
15.9
20.5
14.6
19.0
10.9
12.0
9.2
17.7
6.8
1.7
9.7
7.6
13.6
11.3
11.6
12.3
14.0
15.3
9.5
6.0
3.2
9.1
7.7
9.6
6.8
3.3
4.1
8.9
12.8
77.7
75.6
76.9
63.7
74.8
72.0
63.6
77.4

-

1.8
1.4
2.1
1.5
3.4

~
-

2.2
2.7
4.3
3.8
3.6
5.7
1.7
3.1
1.8
2.3
2.6
6.8
3.2
2.9
5.5
2.5
2.3
4.8
3.3
7.3
-

-

28.6
34.7
66.0
56.3
62.2
55.8

-

-

5.3
2.6
2.5
9.9
4.4
12.0
5.6
2.8
6.7
7.4
8.9
7.8
5.4
7.4
3.4
9.8
2.7
3.0
5.1
9.8
5.4
5.9
3.6
4.6
5.3
3.6
7.6
11.3
12.6
16.3
6.5
2.9
2.8
1.1
1.8
0.7
2.0
1.4
1.4
1.5
0.9

0.8
1.2

5.7
14.4
28.4
4.2
12.1
9.8
8.5
14.9
6.K
8.2
3.8
8.3
8.2
6.7
23.1
2.4
24.3
24.9
6.1
2.7
1.9
8.4
9.1

-

-

34.3
23.0
27.1
28.2
31.8
49.8
32.1
25.0
28.2
20.7
23.3
14.2
23.4
16.6
11.9
20.7
12.9
10.9
23.8
22.9
7.0
5.7
42.7
23.5
18.7
11.0
40.8
26.2
30.9
28.3
14.7
4.2
2.7
11.5
10.6
17.0
8.9
2.4
1.7
2.3
3.6
3.1
5.1
6.7
8.7
7.9
10.3
15.5
12.2

8.3
3.9
2.2
7.4
2.8
8.5
6.4
2.5
6.9
2.6
6.0
4.1
4.3
6.6
1.6
5.9
1.1
2.6
3.9
6.2
3.4
2.3
9.6
6.8
6.3
1.8
11.5
10.8
9.7
3.0
1.2
0.8
0.8
-

2.2
3.2
3.6
7.0
9.2

28.9
40.5
23.5
29.3
33.9
33.4
40.7
3X.1
37.6
33.5
44.1
37.0
38.8
40.9
40.4
40.9
44.0
45.0
37.4
64.6
71.2
29.2
53.4
54.2
62.3
22.7
50.2
31.8
27.1
49.9
74.2
90.3
75.4
41.7
68.8
43.0
16.6
26.6
16.9
20.1
19.2
19.3
16.5
25.4
14.0
14.1
13.1
_

_

_

_

_

_

_

1.3
-

_

_
-

-

–
-

-

-

3.1
-

-

1.1
2.0

_

1.2
_

_

_

-

_
-

_
_
_
_
_
_
_
6.5
2.3
10.2
9.8
8.2
6.7
-

_
_

_

_

_

_
_
_

_
_
_

_
_
_

–
_
_

-

1.7
1.5

_

_
_
_
_

9.9
7.8
_
0.9
_

-

o

_
_
_
_
11.5
0.9
2.9
3.2
3
.
1.6
_
_
_
_
_
_
_

.
.
_
_
_
_

_
_
_
_
_

9
0.9
1.8
6
0
_
_
_

_
1
1
_
_
_
_

_
_
_
_
_

.
-

-

-

_
_
_
_
_

_
_
_

_

_

_

_
_
-

_

_
-

-

-

-

_
_
_
_
_
_
_
_
-

-

_
-

1

_

_
Trace

4.9
_
_
_
_
_
_
_
_
_
_
_

_
_
_
_
_

-

-

-

-

_

_

-

-

-

_

_
-

_
_
_
_
_
_

-

_
_

Trace
_

_
_
_

_
_

_

_

_

-

_

-

-

-

-

-

_
_
_

_

_
_

_
_

_
_
_

_

_
_

_
_

_
_

_
_

_
_
_
_

_
Pres.
_
_
_

Peakat 12.1 A.
Peak at 3.14 A.
Peakat 7.12 A.

H
W
LO
00

o

SITE 210

APPENDIX D
Thermal Conductivity Measurements, Site 210

386

Core,
Section,Interval
Below
Top (cm)

ThermalConductivity(mcal/°C cm sec)

Standard
Deviation

Ambient
Core
Temperature(°C)

1-3,70
1-5,702-3,75
3-3,703-5,70
6-3,708-3,708-5,70
9-3,70
9-4,7010-2,75
10-4,75
11-2,80
12-2,75
12-3,75
12-4,75
13-2,75
13-2,75
14-3,75
20-4,78
21-3,82
22-3,73
22-5,66
23-2,64
23-4,64
24-3,66

0.002412
0.002276
0.002852
0.002347
0.002331
0.002379
0.002695
0.002558
0.002814
0.002818
0.002500
0.002716
0.003077
0.003010
0.002710
0.002717
0.002841
0.002851
0.002900
0.002420
0.002588
0.002733
0.003095
0.003332
0.002945
0.002823

0.009030
0.008443
0.012824
0.007474
0.009682
0.012060
0.009504
0.005861
0.009778
0.007347
0.004362
0.008852
0.006794
0.009394
0.011006
0.007382
0.006038
0.009001
0.010254
0.006976
0.007547
0.005181
0.009423
0.005962
0.006008
0.007399

21.50
23.55
20.64
20.40
21.33
24.07
23.06
24.08
23.16
24.30
21.67
22.76
21.24
21.62
22.60
22.24
21.01
23.06
22.75
24.02
24.71
23.39
23.87
21.93
21.57
22.37

24-5,65

0.002955

0.006521

23.10

25-3,700.002884

0.004803

22.87

27-3,700.002940

0.007624

23.71

28-3,700.003472

0.007499

22.55

28-5,74

0.003483

0.004373

22.67

29-4,60
30-2,67
30-3,031-1,032-3,89
33-3,100

0.003589
0.003348
0.003002
0.002927
0.002880
0.002657

0.005649
0.010471
0.013605
0.004705
0.014372
0.003393

23.24
22.40
19.89
21.79
23.06
21.78

Remarks

RepeatDrilledhole infirm clay
Drilledhole infirm clay
Drilledhole infirm clay
Drilledhole infirm clay
Drilledhole inchalk
Drüledhole infirm clay

Site 210

Cored Interval; 0-9
FOSSILCHARACTER

Hole

Core 2

Cored Interval; 9-18 m

FOSSILCHARACTER

LITHOLOGIC DESCRIPTION

LITHOLOGIC DESCRIPTION

Graded cycles of silt and clay with interbeds
of biogenic ooze.
Nearly 3 of the lower 4 m of Core 1 are so
disturbed that Individual graded cycles cannot
be noted in detail. The less disturbed 6 m
contain approximately 30 graded cycles with anaverage thickness of about 15 cm and a range inthickness from about 3 to 30 cm. Twenty-fourof the cycles have silt bases, many in erosional
contacts with the underlying beds. Most of thecycles are shades of olive gray and greenish
gray. Usually the cycles are darker at the baseand lighter at the top. The upper 47 cm of thecore is yellowish brown.
Eleven interbeds of bluish white and greenish
gray πanno and foram ooze were noted. They
average about 11 cm in thickness and range
from 2 to 20 cm.

Graded cycles of silt and clay with interbeds
of nanno ooze.
Nearly 2.5 m of Core 2 are so disturbed that
individual graded cycles cannot be noted indetail. The less disturbed 6.5 m containapproximately 14 graded cycles with an average
thickness of about 25 cm and a range in thickness
from about 12 to 50 cm. Eight of the cycles havesilt bases, many in erosional contacts with theunderlying beds. The cycles are mainly shades ofolive gray and greenish gray. Usually the cycles
are darker at the base (olive black) and lightening
toward the top.
Eleven interbeds of biogenic ooze (mostly nannos)
were noted. They average about 19 cm in thickness
and range from 3-42 cm. Most are light-greenish
gray.
Mineralogy similar to Core 1.

Generalized Mineralogy for Cores 1-30
Graded cycles of silt and clay:
Mainly subangular quartz and Plagioclase,
mica, and calcite plus aragonite. Calcareous material is mainly forams inthe basal portions of the cycles andnannos in the upper portions. Minor
constituents present in varying amounts
include chlorite, altered glass?, plantdebris, clay minerals, tunicate sclerites,
amphibole, zeolites, potash feldspar,and pyrite.
Interbeds:
Mainly nannos with varying amounts offorams, clay minerals, and clay-size
particles.

The numbers along the l e f t margin of the
Lithologic Description column refer to thenumber of graded cycles of s i l t and clay inthe indicated intervals and the number ofinterbeds of biogenic ooze (in parenthesis).
These same symbols are used through Core 30.

Core
Catcher

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Core
Catcher

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Site 210
I

Hole
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Core 3

FOSSIL I
CHARACTER

w —II
ö

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Cored Interval: 18-27 m
I

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. 5

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LITHOLOGY

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Si

About 4 m of Core 3 areso disturbed that
individual graded cycles cannot be noted indetail. The less disturbed 5 m containapproximately 14 graded cycles with an average
thickness of about 28 cm and a range in thickness from about 7 to 58 cm. Ten of the cycleshave silt to sandy silt bases, many in erosional
contacts with the underlying beds. The cycles
are mainly shades of olive gray and greenish
gray. Usually the cycles are darker at the base(olive black) and lightening toward the top.
Five interbeds of nanno ooze were noted. They
average about 28 cm in thickness and range from
7 to 50 cm. Most are light greenish gray.
Mineralogy similar to Core 1.

_l_

_l

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d

α

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cQ

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2

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LITHOLOGY

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Site 210

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Core

Core 5| FOSSIL | I

Cored Interval: 36-45 m

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I

CHARACTER
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LITHOLOGYg- :zr÷--r:jr:. 4

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CC

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Graded cycles of s i l t and clay with interbeds
of nanno ooze.
Core is too disturbed for any bedding d e t a i l s
to be noted. Colors range from light greenish

1.0—~-~-•~—~-~-

Mineralogy similar to Core 1.

2: ---------

2

XM-__._.._.
3
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LITHOLOGIC DESCRIPTION- 1"-"."."U~-'- ..^ '~•J~—
0.5—_—_-_-_-_•;_..-•- _.:_.T:.-^.-I:
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LITHOLOGIC DESCRIPTION:..---..-•~r.~"

C a t c h e r

4

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to

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Z -~•-~•-~-~—~. »- '÷"•_."_
1.0— ..—"-"—"U7!
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Cored Interval: 27-36 m

I

LITHOLOGIC DESCRIPTION

Graded cycles of silt and clay with interbeds
of nanno ooze.

E ^ ^
N

Core 4CHARACTER- •_r."_'~lT_"
0.5—-•- '-~-~-~-~—- '.—-~-~-~- '.'-~.'S~.-7.'-~.'I r•^-.-l---.-~. .

HoleI DOSSIL I

6 S

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1

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Core 6FOSSIL I

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Cored I n t e r v a l : 45-54 m

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Core 8FOSSIL I

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LITHOLOGIC DESCRIPTION

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g

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B

4

ε I i *"
Graded cycles o f s i l t and clay w i t h interbeds
of nanno ooze.
Core is too disturbed for any bedding details
to be noted. Colors range from light greenishra
9 y to dark greenish gray to olive black.
Mineralogy similar to Core 1.

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Cored Interval: 54-63 m

CHARACTERöMineralogy s i m i l a r to Core 1 .

CatcherCore 7I•: "-~_•~-".-":r_~_~_~n~

I FOSSIL I

Four interbeds of nanno ooze were noted. They
average about 4 cm in thickness and range from
2 to 6 cm. They are mostly l i g h t greenish grayto yellowish gray.

Z'.7.'-~.--.-7:-~. 4_

Catcher

Hole

Graded cycles of silt and clay with interbeds
of nanno ooze.
The upper 4.6 m of Core 8 are so disturbedt h a t i n d i v i d u a l graded cycles cannot be noted
i n d e t a i l . The less disturbed lower 2 m containapproximately 15 graded cycles w i t h an average
thickness of about 12 cm and a range i n thickness
from about 3 to 20 cm. Nine of the cycles haves
ü t to s i l t y sand bases, many 1n erosional
contacts with the underlying beds. The cycles
are mainly o l i v e black to o l i v e gray to darkgreenish gray, becoming l i g h t e r toward the t o p .
One p y r i t e - r e p l a c e d worm burrow cast occurs
about 85 cm above the base of the core.

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LITHOLOGIC DESCRIPTION

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Z'-'-'.'-'.-'.'Z'-~•'-~•'-7~-~- ••_;—•-:T_.-."_.._Z ;1_"_~."- •—""-• •'-"-"Z'•-~•-~-~~~'_,.._.
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Cored I n t e r v a l : 63-72 m

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LITHOLOGIC DESCRIPTION

Graded cycles o f s i l t and clay with interbeds
of nanno ooze.
c° r e is too disturbed for any bedding details
to be noted. Colors range from very light grayto dark greenish gray.

Mineralogy similar to Core 1.

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S i t e 210

HoleCore 9

Cored I n t e r v a l : 72-81 m

Core 10FOSSILCHARACTER

Cored I n t e r v a l ; 81-90 m

FOSSILCHARACTER
LITHOLOGIC DESCRIPTION

LITHOLOGIC DESCRIPTION

Graded cycles of silt and clay with interbeds
of nanno ooze.
The upper 2.1 m of Core 9 are so disturbedthat individual graded cycles cannot be noted
in detail. The less disturbed lower 3.5 m
contain approximately 21 graded cycles with anaverage thickness of about 13 cm and a range inthickness from about 2 to 43 cm. The thicknessof the graded cycles is much less in the lower
62 cm of the core. There 9 cycles average about
3 cm in thickness. The upper 2.9 m of the lessdisturbed portion contain 12 cycles averaging about
20 cm in thickness. Nearly all the cycles havesilt to sandy silt bases in erosional contacts
with the underlying beds. The cycles are shaded
olive gray to dark greenish gray to greenish gray.
One pyrite-replaced worm burrow cast occurs about
45 cm above the base of the core.
Ten interbeds of nanno ooze were noted. They
average about 8 cm in thickness and range from 3
to 17 cm. Most are very light gray and lightgreenish gray.
The disturbed portion of Section 2 contains avery light gray area of foram ooze which might
be graded.
Mineralogy similar to Core 1.

Graded cycles of silt and clay with interbeds
of nanno ooze.
The upper 4 m of Core 10 are so disturbed that
individual graded cycles cannot be noted indetail. The less disturbed lower 1.35 m containapproximately 9 graded cycles with an average
thickness of about 12 cm and a range in thickness
from about 5 to 38 cm. Seven of the cycles havesilt bases, most in erosional contacts with theunderlying beds. The thickest of the graded cycles
is unusual in that it is composed almost entirelyof nannos anf forams. The other cycles are
predominantly of nonbiogenic constituents, mostly
silty clay and clayey silt. Most of the cycles
are olive black to dark greenish gray to lightgreenish gray.
Five interbeds of nanno ooze were noted. They
average about 4 cm in thickness and range from
1 to 8 cm. Most are very light greenish gray.
Mineralogy similar to Core 1.

2
~ 1

(3)
Core
CatcherCore
Catcher
Hole
FOSSILCHARACTER

Core 11

Cored Interval: 103-112 m

LITHOLOGIC DESCRIPTIONCoreCatcher

Graded cycles of silt and clay with an interbedof nanno ooze.
The upper and lower portions of Core 11 are so
disturbed that individual graded cycles cannot
be noted in detail. The less disturbed middle
0.9 m contain approximately 5 graded cycles
with an average thickness of 17 cm and a range
in thickness from 5 to 21 cm. All the cycles havesilt to silty sand bases, most in erosional
contacts with the underlying beds. The upper 3
cycles are much richer in biogenic constituents
than most of the other cycles in the basin. They
are greenish gray to yellowish gray. The twolower cycles are more typical, being mainlycomposed of noncalcareous detritus and ranging
in color from olive gray to dark greenish gray.
One 5 cm thick interbed of yellowish graynanno ooze was noted.
Mineralogy, except as noted above, similar
to Core 1.

S i t e 210

HoleCore 12

Cored I n t e r v a l . 1 2 2 - 1 3 1

S i t e 210

FOSSILCHARACTER

Hole

Cored I n t e r v a l : 159-168 m

FOSSILCHARACTER
LITHOLOGIC DESCRIPTION

LITHOLOGIC DESCRIPTION

Graded cycles of silt and clay with an underlying bed of nanno ooze.
Approximately 22 graded cycles occur in Core
12. They average about 26 cm in thickness andrange in thickness from about 5 to 110? cm. They
all have silt bases, most in erosional contacts
with the underlying beds. The cycles are olive
black to dark greenish gray to greenish gray(darker at the base, lighter at the top).
Two pyritized worm burrow casts occur in
Section 2.
One 30 cm thick greenish gray bed of nanno ooze
occurs at the bottom of the core.
Mineralogy similar to Core 1.

Graded cycles of silt and clay with interbeds
of nanno ooze.
Approximately 9 graded cycles occur inCore 14 (the number is very approximate
because interpretation is difficult inthe more disturbed portions). They average
about 33 cm in thickness and range fromabout 8 to 65 cm. They all have silt bases,
most in erosional contacts with the underlying beds. The cycles range in color from abase of olive black or dark greenish grayto a top of various shades of greenish gray.
Two interbeds (3 and 8 cm thick) of lightgreenish gray nanno ooze were noted.
Mineralogy similar to Core 1 except much of
the sequence is rich in zeolites.

TION

Core
CatcherA

LITHOLOGIC DESCRIPTION

2

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to

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Foram ooze and graded cycles of silt and clay.
The upper 55 cm of Core 13 is very light grayforam ooze. Underlying this is a 10 cm bed ofbluish white nanno ooze typical of the interbeds
between graded cycles of silt and clay. Underlying these biogenic deposits are approximately
11 graded cycles averaging about 21 cm in thickness and ranging from about 2 to 40 cm. Four
graded cycles in the lower 20 cm of the core
average about 3 cm in thickness whereas theoverlying 7 cycles average about 31 cm. Eightof the cycles have silt bases, most in erosional
contacts with the underlying beds. The bases of
the cycles are mostly olive black and olive
gray grading upward into various shades ofgreenish gray.

0.5-

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Core
Catcher

LITHOLOGY

DEFORMATION

α:

NN17

DEFORMATION

LITHOLOGY

NN18

LATE PLIOCENE

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Cored Interv al: 40-149 m
LITHO.SAMPLEoεCore 13
METERSHoleF DSSI L
CHA RAC1 ERSECTION

ZONE

AGE

Site 210

LATE PLIOCENE

LJ-

Cored Interval: 178-187 m
LITHO.SAMPLE

ασ

METERS

ZONE

AGE

Core
Catcher

SECTION

Core 15
F DSSI L
CHA RAC ER

LITHOLOGIC DESCRIPTION

Graded cycles of silt and clay with anunderlying bed of nanno ooze.
Approximately 7 graded cycles occur inCore 15. They average about 17 cm in thickness
and range from about 7 to 28 cm. They all havesilt, bases, most in erosional contacts withthe underlying beds. The cycles are olive
black to olive gray at the base to greenish
gray at the top.
One 28 cm thick light bluish gray bed ofnanno ooze occurs at the bottom of the core.
Mineralogy is similar to Core 1.

C/3
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Core 16iu_

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Site 210

Cored I n t e r v a l ; 198-206 m

F3SSI LLITHOLOGY

HoleCore 19

Cored I n t e r v a l ; 253-262 m

FOSSILCHARACTER

DEFORMATION
LITHO.SAMPLE

Site 210

LITHOLOGIC DESCRIPTION

LITHOLOGIC DESCRIPTION

EMPTY

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NN17

LATE PLIOCENE

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Core
CatcherRüi

Graded cycles of s i l t and clay with interbeds
of nanno ooze.
Approximately 4 graded cycles occur i n Core
16. They average about 15 cm in thickness
and range from about 4 cm to 21 cm. They a l lhave s i l t bases, most in erosional contacts
with the underlying beds. The bases are o l i v egray to o l i v e black with the toDS various
shades o f greenish gray.
Two 6 cm thick interbeds of l i g h t greenish
gray nanno ooze were noted.
The lower 37 cm of the core i s a dark greenish
gray bed of nongraded s i l t y c l a y .

17 (8)

Mineralogy s i m i l a r to Core 1 .

Site 210

1
1

Cored Interval; 215-224 m

Hole
FOSSILCHARACTER

Graded cycles of silt and clay with interbeds
of nanno ooze.
The upper 25 cm of Core 19 is downhole
contamination. The underlying 80 cm is highly
disturbed and mixed silt, clay, and ooze. The
lower 1.5 m of Core 19 contain approximately
21 graded cycles averaging about 5 cm in thickness and ranging from about 1 to 17 cm. The
cycles have silt bases, some in erosional
contacts with the underlying beds. The cycles
are various shades of greenish gray (darker
at the base, lighter at the top).

DOWNHOLEQNTAMINATIOCore
Catcher
LITHOLOGIC DESCRIPTION

One 3 cm thick grayish olive bed of crosslaminated silty sand occurs 90 cm above the bottomof the core.
A 2 cm chunk of pyrite occurs 40 cm above
the bottom.
Twelve interbeds of light greenish graynanno ooze were noted. They average about
2 cm in thickness and range from <l to 8 cm.
Mineralogy similar to Core 1.

Cored Interval: 272-281
FOSSILCHARACTER

I 1
3
— 2

Graded cycles' of silt and clay with interbeds
of nanno ooze.
Approximately 10 graded cycles occur in Core
17. They average about 17 cm in thickness andrange from about 2 to 75 cm. They all havesilt bases, most in erosional contacts withthe underlying beds. Most of the bases aredark greenish gray grading upward into various
lighter shades of greenish gray.
Four interbeds of greenish gray to lightgreenish gray nanno ooze, were noted. They
average about 5 cm in thickness and range
from about 3 to 7 cm.
Mineralogy similar to Core 1.

LITHOLOGIC DESCRIPTION^
2

12 (4)
7 (2)
4

Core
Catcher

12 (2)Hole
FOSSILCHARACTER

Core 18

Cored Interval; 234-243 m

Graded cycles of silt and clay with interbeds ofnanno ooze.
The upper 4 m of Core 20 contain approximately
47 graded cycles averaging about 5 cm in thickness and ranging from about 2 to 18 cm. Mostof the cycles have silt bases and many are inerosional contacts with the underlying beds.
The cycles are mostly shades of greenish gray(darker at the base, lighter at the top).
^ne ^ cm thick bed of medium gray and greenish
gray laminated and cross-laminated silty sandcomposed mainly of quartz and forams occurs near
the middle of the core.
Twenty interbeds of white and light greenish
gray nanno ooze were noted. They average about
6 cm in thickness and range from <l to about
23 cm.
The lower 1.5 m is so disturbed that individual
graded cycles cannot be noted in detail.

laminatedsilty sand
LITHOLOGIC DESCRIPTION

Mineralogy similar to Core 1.
8 (4)Graded cycles of silt and clay with interbeds ofnanno ooze.

Core
Catcher

1 reversely?
1
Core 18 contains two normally graded cycles
1of 20 and 13 cm thicknesses and 1 reversely?
graded bed of 5 cm thickness. The normal cycles
have silt bases grading upward into clayey silt
and silty clay. The bases are dark greenish grayand the tops greenish gray.
Two 5 cm thick interbeds of light greenish graynanno ooze were noted.
Mineralogy similar to Core 1.

Core
CatchertoI—'OS i t e 210

S i t e 210

Cored I n t e r v a l : 2 9 1 - 3 0 0 m

Hole

Hole

Cored I n t e r v a l : 309-318 m

FOSSILCHARACTERFOSSILCHARACTER
LITHOLOGIC DESCRIPTION

_ 1

I 2

I 3 [2)

Nanno ooze and interbeds of clay.
Graded cycles of silt and clay with interbeds
of nanno ooze (semilithified).
The upper 2.7 m of Core 21 are mainly bluishwhite nanno ooze (chalk) with 5 interbeds ofgreenish gray very slightly to moderately
calcareous clay and silty clay. The clay beds
average about 15 cm in thickness and one ofthem is graded. Much of the nanno ooze and clay
are burrowed (chondritcs).
The lower 1.5 m of Core 21 contain approximately
13 graded cycles averaging about 7 cm in thickness and ranging from 2-15 cm. Seven of thecycles have silt bases, some in erosional
contacts with the underlying beds. The cycles
are olive gray or dark greenish gray at thebases and lighter greenish gray at the top.
Eleven interbeds of bluish white and lightgreenish gray nanno ooze were noted. They
average about 4 cm in thickness and range
from about 1 to 11 cm.
Mineralogy similar to Core 1.

LITHOLOGIC DESCRIPTION

Graded cycles of silt and clay with interbeds
of nanno ooze (stiff to semilithified).
Approximately 31 graded cycles occur in Core 22.
They average about 14 cm in thickness andrange from about 4 to 55 cm. About half havesilt bases, many in erosional contacts with theunderlying beds. Almost all are shades ofgreenish gray (darker at the base, lighterat the top).
Nineteen interbeds of mainly greenish grayand light greenish gray nanno ooze werenoted. They average about 6 cm in thickness
and range from about 2 to 23 cm.
Mineralogy similar to Core 1.

3 (2)

- 1
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Catcher- 2

S2
Site 210
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Core 23

Cored Interval:328-337 m

I

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LITHOLOGIC DESCRIPTION

tt

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Nanno clayey s i l t to Nanno s i l t y clay.
Calcareous sandy s i l t .
( s t i f f to Semilithified)i.o- :"_:::"._•"._")One graded cycle about 2 m above the base of theo r e is particularly rich in forams and islaminated and cross laminated(?).
Twenty-five interbeds of nanno ooze were noted.
Ma" y a r e s l i g h t l y t o i n t e n s e l y burrowed (someChondrites).
Most beds a r e l i g h t greenish grayt o g r e e n l s n g r a y - A5 O u t one t h i r d a r e b l u i s hwhite and l i g h t bluish gray, including the
thicker beds. The overall average thicknesst,out 10 cm and the range is from about 2 to4^ 0s cam

2

" ;L~'_"_ri;".•
I••'.'.'-.'.-..-~.-~- '.~_'.~r.~_'.~_'.~- L~÷-•~—'.'.'_ '.'÷~-T.-~.lT._- ••_-_-_-•_-"—~-~The upper 8.5 m of Core 24 consist mainly of
nanno clayey s i l t to nanno s i l t y clay. Someportions are richer in nannos and more properly
called nanno ooze. Whereas other portions arepoorer in nannos and more properly called s i l t y
clay and clayey s i l t . Megascopically, the clay
is homogeneous and no grading was detected.
Color is greenish gray to dark greenish gray.

- \^~~".'JZ^7~L- lT_~._r_~_~ j

XM~ 'Z7.Z7.-7.~S7.•••-••- "7.-..-7.Z7.-7.
—.._ toMineralogy similar to Core 1 except that someof the graded cycles are zeolite r i c h .

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Pyritized globs (worm burrow casts) are foundin Sections 3 and 4 (one in each).
Underlying the upper beds w i t h g r a d a t i o n a l
c o n t a c t a r e 40 cm o f t h i n l y laminated o l i v egray calcareous sandy s i l t .

M
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LITHOLOGIC DESCRIPTION—I I

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LITHOLOGY

I

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Graded cycles of silt and clay with interbeds(stiff to Semilithified).
Approximately 48 graded cycles occur in Core 23.
They average about 12 cm in thickness and range
from about 2 to 74 cm. About two thirds havesilt bases, many in erosional contacts with theunderlying beds. Almost all are various shades ofgreenish gray (darker at the base, lighter at
the top).

l

c

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Cored Interval.- 347-356 m

IS
S

of nanno ooze*
I

I

CHARACTER
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Core 24

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Core 27

Cored Interval:365-374 m

LITHOLOGIC DESCRIPTION

LITHOLOGIC DESCRIPTION

Silty sand and sandy silt.
Graded cycles of silt and clay with interbeds
of nanno ooze.
(stiff to semilithified)
The upper 53 cm of Core 25 is laminated andcross-laminated olive gray silty sand mainlycomposed of altered glass?, quartz, feldspar,and forams. About 1.35 m further down is a
15 cm thick bed of laminated light olive graycalcareous sandy silt.
The rest of Core 25 consists of graded cycles
and interbeds of nanno ooze. Approximately 42
graded cycles occur, averaging about 10 cm inthickness and ranging from about 3 to 22 cm.
Nearly half have silt bases, some in erosional
contacts with the underlying beds. Most of thecycles are shades of olive gray and greenish
gray (darker at the bottom, lighter at the top).
Two of the graded? cycles appear to be laminatedin their lower portions.
Sixteen interbeds of mostly light greenish grayand greenish gray nanno ooze were noted. They
average about 6 cm in thickness and range fromabout 2 to 24 cm. Many are worm burrowed withworm burrow casts of the overlying lithology(some chondrites types and Zoophyaos? types).
Mineralogy similar to Core 1 except as noted
above.

Graded cycles of silt and clay with interbeds
of nanno ooze.
(stiff to semilithified)
Approximately 32 graded cycles occur 1n Core 27.
They average about 17 cm in thickness and range
from about 2 to 65 cm. Nearly all have silt tofine sand bases, many in particularly evident
erosional contacts with the underlying beds.
Most of the cycles are shades of greeenish gray(darker at the base, lighter at the top).
The thickest graded cycle<?) has a 12 cm thick sandy
silt base that is laminated and cross-laminated.
About 6 other cycles have laminated bases, one ofwhich is also cross laminated.
The upper portions of some of the cycles areburrow mottled.
Fourteen interbeds of light greenish gray,greenish gray, and bluish white nanno ooze werenoted. Many are slightly to intensely burrowed(some Chondrites and Zoophyaoβ types). Burrow
casts are often a mixture of the host lithology
and the overlying lithology. The interbeds average
about 10 cm in thickness and range from about
2 to 21 cm.
Mineralogy similar to Core 1.

Core
CatcherCore 26

Cored I n t e r v a l : 84-393 m_
A

P

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FOSSILAGE
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LITHOLOGY

DEFORMAT

Hole

LITHO.SAM

S i t e 210

Cored Interval: 403-412 m

FOSSILCHARACTERFOSSILCHARACTER

LITHOLOGIC DESCRIPTIONCoreCatcherCore
CatcherON

Site 210

I

HoleCore 28

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The lower 5.1 m of Core 28 is mainly a sequence
9 r a d e d cycles and interbeds of nanno ooze.
Approximately 25 graded cycles occur averaging
about 12 cm in thickness and ranging from about3
to 28 cm. Nearly all have fine sand to siltbases in erosional contacts with the underlying
beds. Most cycles are shades of greenish gray(darker at the base, lighter at the top). Someof the darker basal color is due to the presence"f carbonaceous material. About 10 of the cycles
have laminated bases (2 of which are also crosslaminated). These bases also show particularly
good evidence of scouring the underlying beds.

N A P

Thirteen interbeds of nanno ooze were noted.
Most are various shades of greenish gray, someare bluish white. Most are burrowed with about"alf containing Chondrites and several Zoophycos.
The interbeds have a median thickness of about
11 c m a n d range from 3 to 57 cm.

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Mineralogy similar to Core 1 except bases ofcycles are more micaceous.

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LITHOLOGIC DESCRIPTION

XM

3"_-_-_"""_-_.___.__-_"_"_""_'

r-_-i-_-_i

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(

bio

geπic)

1

Nanno ooze and interbeds of noncalcareous clay.
Graded cycles of s i l t and clay with interbeds
of nanno ooze.
(Semilithified)t M H I Y,-—•=T —.
Z ~L"_L_"L"_i_~1

The upper 2.85 m of Core 29 are about 75 percent
nanno ooze and about 25 percent composed of 7interbeds of noncalcareous clay and silty clay
' n o t o b v i ° u s l y graded). The interbeds average
about 12 cm in thickness and range from about
5 to 25 cm. The nanno ooze varies from white togreenish gray depending on the clay content(more clay producing darker colors). I t isintensely burrowed in some portions (somechondrites).
The i n t e r b e d s a r e dark greenish
9>"ay s°me s l i g h t l y mottled.

I. _l_ _i_l~_i_"'~_l_:~ ~•- ~j|^jZ•-., ^- -L ÷ L . ~— ^_-_-_^_-_----r- r~ ' • '—~ -l^"I-"J^-_r-_;

The lower 5.22 m of Core 29 are mainly a sequence° f graded cycles and interbeds of nanno ooze.
Approximately 13 graded cycles occur. They average
about 12 cm i n thickness and range from about
3 to 32 cm. Nearly a l l cycles have fine sand ors i l t bases, many in erosional contacts with theunderlying beds. The cycles are mostly shadesof
9 r e e r | i s n g r a y (darker at the base, lightera*• " l e t o p ) . Several o f t h e c y c l e s have l a m i n a t e d

F

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The upper 2.7 m of Core 28 are essentiallyvery light gray to bluish white nanno ooze
with some portions bearing clay and forams.
g n e j c m ^ n ic|( becj of dark gray noncalcareous
clay occurs near the top of the core. Burrowing
is slight to intense in various portions of
the ooze. Some Chondrites types occur.

— _|_ _i_ _L- jL~^-i- -L- J_- L _J_- L -_ L
Z. -i. _i_- -L_i_-L_i_•"•L~ -L _i_ - L- J_~ 1 ~J_" L "_L~ J_~ L •J_" J "_L_ _j_ _i_
- J "_i_" L "_ 1 _~ L
_I J- -I- -•- _i_ _i_ _L~ i -*- | -*- i

6Cored Interval: 440-449 m

I

Nanno ooze,_I ±÷ — ΛJ~"•^±. 1- .• .~_•_^t-• ~ ?r_ .j?Z-:~.
- I"-T•_—_""_~ _._-'~~—.—-—

__

£
UJ

Core 29 •Graded cycles of silt and clay with interbeds
of nanno ooze.
(stiff to Semilithified)

EMPTY

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~ J. j , ,j,_ " ^ _^ _t_
i_ _l_ _ L- j^^-i-^i=r- | -*- , -*- |
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I FOSSIL Iu_;g 5 _I1

Si te 210

Cored Interval: 421-430 m

I

CoreCatcher

One t h i c k (106 cm) i n t e r b e d o f nanno ooze occurs
as well as 4 thinner interbeds of nanno ooze
which average about 10 cm in thickness and range
from about 5 to 15 cm. Most of the ooze i s l i g h t
greenish gray and some is moderately burrowed.
One 5 cm thick l i g h t bluish gray bed of recrystallized limestone occurs in Section 4.
Mineralogy similar to Core 1 except bases are
more micaceous.

TU.T-.~_"-"•..-_-_-_-_:

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Site 210

I

HoleCore 30

I FOSSIL I
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LITHOLOGIC DESCRIPTION

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Cored I n t e r v a l : 4 7 7 - 4 8 6 m

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LITHOLOGIC DESCRIPTIONc l a y-!_•-;• •-, •(Semilithified)- J".r.lT.'_r.'_•~••- ~.'-~.'-~.-~.'-.7'.
-–-7.'JT.-..-7.-..'.
- ~.-7.'-~.'-~.-7..

Cor

e 31 is composed almost e n t i r e l y of darkgreenish gray, s l i g h t l y to moderately mottled,
noncalcareous s i l t y clay and subordinate s i l t y clay.
The upper 35 cm of the core contains two 5 cm
thick beds of l i g h t e r greenish gray foram andquartz rich calcareous s i l t . A 7 cm thick c a l careous bed occurs in Section 4.

2 ~-.^-i-•.

- -~^~~-~-•~-~

3

XM=-:-^-:---1

lower 1.1 m o f Core 30 are i n t e n s e l y d i s t u r b e din some portions. The lithology is mainly lightgray clay bearing nanno ooze interbedded with_!_3

dark greenish gray clay and s i l t y clay. The
oozes are burrowed (some Chondrites) with burrow
casts being dark greenish gray.

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The upper 2.5 m o f Core 30 c o n s i s t o f approximately
7 beds of calcareous biogenic clay and nanno ooze
interbedded with approximately 7 intervals of nongraded calcareous and noncalcareous clay ands i l t y clay. The nanno ooze is very l i g h t gray tol i g h t gray whereas the calcareous biogenic clay
is darker (greenish gray to dark greenish gray).
They are burrowed (some Chondrites), average
about 19 cm in thickness, and range from about
5 to 37 cm. The interbeds are mostly dark greenish
gray, average about 16 cm in thickness, and range
from about 7 to 34 cm.
T" e middle 0.5 m of Core 30 contain approximately
5 graded cycles with two 10 cm thick interbeds
of greenish gray calcareous biogenic clay. The
cycles average about 6 cm i n thickness and range
f r o m about 2 t o 10 cm. They have s i l t bases, somei n erosional contacts w i t h the underlying beds.
The cycles are m o s t l y shades o f greenish g r a y .
y^laminated bases.
jne

U~lirT_~_~_~—"-~'l..'17.-7.'.

rS~_~-~÷~J{uioCore 31FOSSIL I
CHARACTER
I
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-.•.L'. . - .L. .-Nanno ooze and interbeds of clay.
Graded cycles of s i l t and clay with interbeds
of biogenic clay.
(Semilithified)

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S i t e 210

Cored I n t e r v a l : 459-468 m

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Site 210

Hole

Cored Interval; 496-505 m

Cored I n t e r v a l : 515-524 m

FOSSILCHARACTERw

FOSSILto

CHARACTER

LITHOLOGIC DESCRIPTION

5GY4/1LITHOLOGIC DESCRIPTION

10YR4/2
0YR8/2 & 10YR5/4

CLAY, dark greenish gray, s e m i l i t h i f i e d ,moderately mottled, sporadic small (few mm)burrows, i n d i s t i n c t noncalcareous except
for f i n e burrows, not bedded.

CLAY same as 32.
CALCAREOUS SILTvery pale orange + moderate
yellowish brown, s e m i l i t h i f i e d ,intensely burrowed
CLAY moderate yellowish brownto dark yellowish brown, rarespots of moderate reddish brown(10R4/6) to greenish gray
(5G6/1) at Section 2 , 25-35
Section 3, 40-50 Section 4 ,125 moderately but i n d i s t i n c t l ymottled. S e m i l i t h i f i e d , fragments
in d r i l l e d paste.

S e m i l i t h i f i e d but becoming s o f t e r , fragmentsin paste to bottom of core.
_5G4/1
5G6/1

5Y5/2

10YR4/2

Light o l i v e gray to o l i v e gray.

CLAY, yellowish brown with rare greenish
gray (5G6/1) mottles, possibly oxidationreduction phenomenon, s e m i l i t h i f i e d , rockfragments i n paste.

CLAY dark yellowish brownwith l i g h t e r colored burrows,s e m i l i t h i f i e d , moderately
mottled.

10YR8/2

5Y7/2
to
10YR6/2Core
CatcherCore
Catcher

CLAY RICH NANNO OOZE very
pale orange to grayish orange,
moderately mottled darker
burrow f i l l s .
NANNO OOZE, white, t i n t ofpale orange, moderately mottledwith bird's-eye maple liketexture.
CLAY BEARING NANNO OOZE very
pale orange texture likeoverlying
CLAY RICH NANNO OOZE, yellowish
gray to pale yellowish brown,
semilithified.

HoleCore 34

Cored I n t e r v a l : 5 3 3 - 5 4 2 m

Cored Interval:542-551 m

FOSSILCHARACTERFOSSILCHARACTER
LITHOLOGIC DESCRIPTION

LITHOLOGIC DESCRIPTION

5Y6/1- 5YR8/1

CLAY BEARING CALCIC NANNO OOZE
10YR6/2

Pale yellowish brown to greenish
orange and pale yellowish brown.
Intensely mottled, with slightly
darker whisps throughout, distinct
burrows mainly subhorizontal(2-4 mm) rare short steeply
inclined burrows. Semi l i t h i f i e dpieces of rock, fractures inclined
at about 45°.

5Y6/1
and
5YR8/1

CLAY BEARING TO CLAY RICH CALCIC NANNO OOZELight o l i v e gray, w i t h pinkish gray patches
and lenses scattered throughout, semi l i t h i f i e d ,moderately mottled showing b i r d ' s - e y e maplel i k e t e x t u r e , m o t t l i n g most conspicuous i n
Section 4. Some suggestion of bedding, dip 20°.
Some steeply i n c l i n e d cracks. Occasional chert
nodules to 2 cm ( o l i v e gray 5Y4/1) in Section
1, 145-150 cm, Section 3 15-25, 55, 88, 124,
Section 4 72, 138.

Average of about 85% carbonate in core.

— 5YR8/1

Bands and patches of pinkish
gray (5YR8/1).
5Y6/1

—

5Y8/1
gradational
5YR8/1Pa1er

patches absent.

Average of about 90* carbonate in core.
10YR8/2Core
CatcherCore
Catcher

CΛ
H
W

4^

8

Cored I n t e r v a l ; 5 5 1 - 5 6 0 m

Hole
FOSSILCHARACTERFOSSILCHARACTER

Core 37

Cored Interval;560-569 m

LITHOLOGIC DESCRIPTION

grading
to
5GY9/1

grading
~_iG"

C

to

LITHOLOGIC DESCRIPTION

CLAY RICH CALCIC NANNO OOZE
Very l i g h t yellowish gray grading intol i g h t greenish gray, semi l i t h i f i e d ,moderately but i n d i s t i n c t l y mottled,forams sparsely present from Section 2,
50 cm. Moderately to steeply inclined
fractures with slickensides. I n d i s t i n c tlayering dipping at up to 15°. Bands
with glauconite in Section 2 and top
15 cm of Section 3, possible zeolites
Sections 3-5.
o<->oAverage of about 75% carbonate.
Calcic rich nanno clay.
Average of about 55% carbonate.

and
5G6/1

FORAM BEARING NANNO RICH CALCIC CLAY
Very light greenish gray to greenish gray,with some darker bands and patches. Semilithified, moderately mottled, burrows indistinct.
Semilithified, fractures and minor faults dipping
45-70°. ?bedding dips 0-10°. Pale purple mineralon slickensides Section 3 20-22 cm. (5P6/2)
Forams sparsely distributed throughout, rare
bluish purple specks (?pyrite).
Average of about 60% carbonate in core.

and
5G9/1

grading
to
5G7/1

c
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5G8/1

c
c

533'"
and
5G6/1

c
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pale green 10G6/2

c
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Core
CatcherCore
CatcherSite 210

I

HoleCore 38

I FOSSIL I

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Cored I n t e r v a l : 569-578 m

Site 210

I II

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CHARACTER

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Cored I n t e r v a l : 587-596 m

I

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CHARACTER

ui

LITHOLOGIC DESCRIPTION>;r•;/i

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LITHOLOGY^I

HLH"'"•i-1-"_l_'~rJ-jLirQJ-~_j_;r-*-_"- 1 - i~•-

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Core 40

EMPTY

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I FOSSIL I

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LITHOLOGIC DESCRIPTION

H-

EMPTY

—-.^—π—.
. j -i Q

CALCIC RICH NANNO CLAY
Lithology similar to Cores 38 and 39.

0 5J

CLAY RICH CALCIC NANNO OOZEGreenish gray, S e m i l i t h i f i e d , moderately
mottled, very fine forams, layering dips
about 10°.
At 105 color changes to very pale blue
green, pale blue green and l i g h t greenish
gray with pale purple (5P6/2) patches
around black cores ( p y r i t i c ) i n burrows.

i o-^Jac ]—^lè

Few flr a c u r e st

Average of about 65% carbonate in core.

5GY8/22

5BG8/2c

Z. ~.'-~.. J.
- —-- -*-_! cz '-'--- '•J-_i

Layering more d i s t i n c t i n Section 2 ,dips 5 to 10°.
1

to::r_: j_-J

Site 210

I
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core
Catcherp

HoleCore 39

I FOSSIL I
S

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Z~•-~•-~-i-~_• •j_;.'"-"..
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5BG8/2:

to

CALCIC RICH CLAY NANNO OOZEV P a l ? blue green to l i g h t greenish gray.
S e m i l i t h i f i e d , moderately mottled, pale
purple patches (5P6/2) around black cores(pyritic?) in burrows, few fractures inclined
at about 45°, a few darker bands (purple t i n t ) ,sparsely scattered forams.

5GY8/1
XM
CC

-

-*-J

Average of about 65% carbonate i n core.

^fcc: " • _ T i __i__—fL- __.. _J__
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I I | ICP5_.^_J-jGreenish gray (5G6/1) patches- :..17|_L .

(concretionary) a t 60, 87, 104.

I~J-i °
It.

Average of about 55% carbonate 1n core.

- «j?%S^.jVs^~ "JöSQ ç>^^"Gravel produced by drilling variety oflithologies present back to those in

IIR

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Fractures subhorizontal .

Ver

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Broad banding.
.

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Layering less distinct a few fractures(slickensided) inclined at 30-45°.

LITHOLOGIC DESCRIPTIONI

E M P T Y

0.5^

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ö

crvH/i
8
/1

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m
λ

Cored I n t e r v a l : 578-587 m

I

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- ~ . J - j ,5GY8/1"-!-"-.-

CHARACTER
=i

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5BG7/2r

N"-~N

NANNO BEARING CLAY CALCIC OOZE

:-"-

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I

Site 210

to

Hole

Site 210

Cored Interval: 596-605 m

HoleCore 43

H
W

Cored I n t e r v a l ; 614-623

FOSSILCHARACTERFOSSILCHARACTER

LITHOLOGIC DESCRIPTION

LITHOLOGIC DESCRIPTION

5BG7/2
to
5GY8/1CALCIC RICH NANNO CLAY
Lithology similar to Cores 38, 39, 40.
Core mostly broken into short pieces.
Average of about 55% carbonate in core.
Gravel produced by d r i l l ing.
5BG8/2CALCIC RICH NANNO OOZE
Very pale blue green, otherwise appearance
similar to Cores 38 to 42.
Semi lithified, core in short lengths,
slickensided surfaces inclined at 30°,
dip of layering 5-10°.

Pasty material on outside of core.
5BG7/2LITHOLOGY-

DEFORMATION

Cored I n t e r v a l : 605-614

LITHO.SAMPLE

METERSPRES.

ABUND.

ZONEAGE

SECTION

Core 42FOSSILCHARACTERFOSSILEARLY MID EOCENE

Retizulofenestra dictyoda (upper)

A

P

1

CC
XM

1

-L÷Λ
.O~

Average of about 60% carbonate in core.

LITHOLOGIC DESCRIPTIONCoreCatcher

EMPTY

0.5N

JL

5GY8/2tt0

CALCIC RICH NANNO CLAY
Lightology similar to Cores 38, 39, 40, 41.
Core in short pieces a few fractures,dipping at 45°.

a
2

2

F
N
R

A
A

M
P

1 I I I 1 I I II 1 I I I IèCoreCatcher

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121

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C

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Average of about 55% carbonate in core.

l
2

NANNO RICH CLAY CALCIC OOZES i t e 210

HoleCore 44

Cored I n t e r v a l : 623-632 m

Cored I n t e r v a l : 648-657 m

FOSSILCHARACTERFOSSILCHARACTER

LITHOLOGIC DESCRIPTION

LITHOLOGIC DESCRIPTIONCALCIC RICH NANNO CLAY
Ve|r ,y p f l l e b l u e g r e e n > ü t h o l o g y s i m i l a r toCores 38 to 43 1n appearance. S e m i l i t h i f l e d ,dip of layering 5-10°.

FORAH BEARING CALCIC AND NANNO RICH CLAY WITH
5BG7/2Average of about 55% carbonate in core.

5BG7/2with
20% ofbands
of N6

FORAM RICH BANDS
L i t h o l o g i c a l l y s i m i l a r to Cores 38-45,
semil1th1f1ed, s o f t e r sections indicatedby deformation.
Section 1 : foram r i c h a t 37 and 125 cm.
Dip 5 to 10°, weak f l a t f o s s i l i t y .

Section 2: 1 to 5 cm bands r i c h in foram
make up 50% of rock to 100 cm. Darker bands
with more f i n e p y r i t e .

5BG7/2
withSection 3: forams rare to 90 cm,
30%
more common below. Darker bands withbands of fine pyrite.
N6

5BG7/2
with a
few
bands
of N5

Core
Catcher

S i t e 210

HoleSection 4: forams rich 24-25 cm, 27-29,
34-36, 47-48, 49-54, 60-61, 70-72, 87-8
92-93, 105-107, 103-104.

Cored I n t e r v a l : 632-641

LITHOLOGIC DESCRIPTION

5BG8/2

Fragments in paste.
Section 5: 3 foram bands between 90 and 150
5BG8/1cm. Fractures inclined at 45-30°.
with afew
bands of
N6

CALCIC AND NANNO RICH CLAY WITH FORAH RICH BANDS
Very pale blue green to pale blue green.
S e m i l i t h i f i e d , appearance s i m i l a r t o Cores
38 to 44. Foraminifera r i c h bands i n Section 3
at 58-61, 70-72, 88-90 and 147-149 cm.
Dip about 5 ° .
Pyrite nodule f l a t t e n e d in bedding 1nSection 2, 1 cm x 2 cm.

Section 6: scattered forams throughout.
5BG8/2Average of about 50% carbonate 1n core.

Average of about 40% carbonate i n core.

5BG7/2Core

Catcher

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to
h->

o

o
1

Cored Interval: 665-674 m

Site 210

FOSSILCHARACTER

Hole

Core 48

Cored I n t e r v a l : 678-687 m

FOSSILCHARACTER

LITHOLOGIC DESCRIPTION

LITHOLOGIC DESCRIPTIONFORAM BEARING CALCIC RICH NANNO CLAY
Lithology l i k e 46*, forams scattered
Inra/othroughout pale blue green.
*„ , Pyrite crystal clusters at 50, 64, 76Danαs OT ^ t Q 3 ^i n d 1 a m e t e r j
d i p
n e a r10<>N7
to
5B6/1

FORAM BEARING CALCIC RICH NANNO CLAY
Lithology similar to Core 47, l i g h t
gray to very l i g h t bluish gray.
Forams scattered throughout, burrows
mostly f i l l e d with l i g h t o l i v e graysediment (5Y6/1) only infrequently
pyritic.

5B7/1

Section 2: trace of bedding dips about 5°
Fractures inclined at 45° at top of
section (and base of Section 1).

.IT. i_Section 2: softer rock fragments in paste.
5BG7/2
with somebands ofmediumgray N5•J.T_•, E_•" I T i_f•"

Section 3: fewer forams.

Section 3: Sediment s t i f f clay at top of
section grades down into semilithified sediment
below.

Average of about 50% carbonate in core.

Core
Catcher*Burrows mostly f i l l e d with l i g h t olive
gray sediment (5Y6/1) only infrequently
with p y r i t e otherwise'sediments very muchl i k e previous cores.

Section 4: Semilithified to 102 cm. S t i f fpaste below.
Average of about 55% carbonate in core.

Core
Catcher~J.::-

_,

<a:

M

!Λ

2

5B7/1

IOf

s
-

FORAM BEARING CALCIC RICH NANNO CLAY
Light bluish gray, lithology same as Core 48.
Semi lithified.
Section 1: clusters of pyrite crystals at
18 and 36 cm.

~

•

•

-

"

FORAM BEARING CALCIC AND NANNO RICH CLAY WITH
FORAM RICH BANDS
Lithology s i m i l a r to core 49 - l i g h t b l u i s h
gray.

-Si
-•-J

I

1

1.0-

5B7/1

C

1 1 1 Vi

2

LITHOLOGIC DESCRIPTION

c

.

F-•

0.5—

1

02-711 m

1 gSj

LITHOLOGY

DEI

UJ

DNE

UTHOLOGIC DESCRIPTION

Cored I n t e r v a l :Core 50FOSSILCHARACTER

IPLI

Hole

LIT

Site 210

Cored I n t e r v a l : 692-701 m:TION

Core 49

FOSSILI CHARACTER

UNI

Hole

PR,

S i t e 210-'-JSection 1 : s l i g h t l y banded, bedding
i n d i s t i n c t d i p about 10°, forams sparsely
scattered throughout. P y r i t e c r y s t a l s a t 126.

: fi:t^αcj- ÷J~.-i". c
J

Section 2: forams more abundant 80 cm to 150
cm. Soarsely scattered elsewhere.
1

"Fj

I

Section 3: 0-102 cm s t i f f c l a y , 102-146.
Semi l i t h i f i e d fragments i n s t i f f paste.

T

-

pill

EARLY EOCENE

c

3

1

i : i: i: i: i:CoreCatcherN•Py: i : 1 : 1 : 1 : 1

Average o f about 50% carbonate i n core.

dictyoda (lc3—: F-•_-;

2c— .F "

S
O

_-_;
. ..

*=>
.,-

_i

- ~ ~~..

H

c

1

cc

j

. α
-

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Section 4: bedding dips at about 10°,
forams abundant in bands i n upper h a l f ,bands make up 20X of 0-75 cm.
Fine grained p y r i t e band a t 106,
common p y r i t e c l u s t e r at 115.

XM

':"-,

5

Section 3: s e m i l i t h i f i e d except 117-137
which is s t i f f and pasty. Forams abundant
15-23, 81-84, 107-117, sparsely scatteredel sewhere.

c

c

2

1

J

Section 5: s o f t and pasty 0-30 cm,
otherwise s e m i l i t h i f i e d , foram moderately
common throughout, lenses (2mm x 1-2 cm)
o f f i n e p y r i t e at 47, 52, 54, 67, 68,
77 and 83 cm.

c
XT1
1

_L. J

6

:."!'"

. J

c
_1

F
N
R

è

A
C

P
P

Core
Catcher..'J.~(,-1

Section 6: forams common between 10 and 60
cm, f i n e p y r i t e lens at 56. Dip 5-10°, 2
f r a c t u r e s i n c l i n e d a t 45° a t 35 and 55 cm.
Average o f about 40% carbonate i n core.

SITE 210

Ocm

— 25

50

75

100

— 125

150

210-1-1
406

210-1-2

210-1-3

210-1-4

210-1-5

210-1-6

SITE 210
•Ocm

25

I—50

I—75

I—100

I—125

150
210-2-1

210-2-2

210-2-3

210-2-4

210-2-5

210-2-6

407

SITE 210

0 cm

— 25

— 50

— 75

—100

—125

1

150
210-3-1

408

210-3-2

210-3-3

210-3-4

210-3-5

210-3-6

SITE 2100 cm

210-5-1

210-5-2

210-5-3

210-6-1

210-6-2

210-6-3409

SITE 210

0 cm

25

50

— 75

100

125

150

210-6-4

410

210-6-5

210-7-1
210-8-1

210-8-2

210-8-3

210-8-4

SITE 210

•0 cm

25

50

— 75

—100

— 125

150
210-8-5

210-9-1

210-9-2

210-9-3

210-9-4

210-10-1
411

SITE 1100 cm

210-10-2
412

210-10-3

210-10-4

210-11-1

210-11-2

210-12-1

Ocm
SITE 210

210-12-2

210-12-3
210-12-4

210-13-1

210-13-2

2T0-14-1

413

SITE 210

0 cm

25

50

75

100

125

150

210-14-2
414

210-14-3

210-15-1

210-16-1

210-17-1

210-17-2

SITE 210

0 cm

25

50

75

100

125

150

210-18-1

210-19-1

210-19-2

210-20-1

210-20-2

210-20-3
415

SITE 210

0 cm

— 25

— 50

— 75

—100

—125

1

150
210-20-4

416

210-21-1

210-21-2

210-21-3

210-22-1

210-22-2

SITE 210

•0 cm

25

50

75

100

125

150

210-22-3

210-22-4

210-22-5

210-23-1

210-23-2

210-23-3

417

SITE 210

0 cm

— 25

50

— 75

—100

—125

150

210-23-4
418

210-23-5

210-23-6

210-24-1

210-24-2

210-24-3

SITE 210

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210-24-5

210-24-6

210-25-1

210-25-2

210-25-3

—125

419

SITE 210

0 cm

25

— 50

75

—100

—125

150

210-25-4
420

210-27-1

210-27-2

210-27-3

210-27-4

210-27-5

SITE 210

0 cm

— 25

— 50

— 75

—100

—125

150

210-27-6

210-28-1

210-28-2

210-28-3

210-28-4

210-28-5

421

SITE 210

0 cm

25

50

75

100

125

150

210-28-6
422

210-29-1

210-29-2

210-29-3

210-29-4

210-29-5

SITE 210

0 cm

25

50

75

100

125

150

210-30-1

210-30-2

210-30-3

210-31-1

210-31-2

210-31-3

423

SITE 210

0 cm

— 25

— 50

— 75

—100

—125

150

210-31-4
424

210-31-5

210-31-6

210-32-1

210-32-2

210-32-3

SITE 210cm

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SITE 210

0 cm

25

50

75

100

125

150

210-33-4
426

210-33-5

210-33-6

210-34-1

210-34-2

210-34-3

SITE 210

0 cm

— 25

— 50

— 75

—100

—125

150

210-34-4

210-35-1

210-35-2

210-35-3

210-35-4

210-36-1
427

SITE 210

0 cm

25

50

— 75

—100

125

150

210-36-2
428

210-36-3

210-36-4

210-36-5

210-37-1

210-37-2

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210-37-4

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210-38-1

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210-38-2

210-39-1

1"1
210-39-2

429

SITE 210

0 cm

25

50

75

100

I—125

150

210-39-3
430

210-40-1

210-40-2

210-40-3

210-40-4

210-40-5

SITE 210

0 cm

25

50

75

100

125

150

210-40-6

210-41-1

210-41-2

210-41-3

210-42-1

210-42-2
431

SITE 210
0 cm•

— 25

— 75

100

125

150

432

210-43-1

210-43-2

210-43-3

210-43-4

210-44-1

210-44-2

210-44-3

210-4545~1

210-45-2

433

SITE 210

0 cm

25

50

75

100

125

150

210-46-3
434

210-46-4

210-46-5

210-46-6

210-47-1

210-47-2

SITE 210

0 cm

— 25

— 50

— 75

—100

125

150

210-47-3

210-48-1

210-48-2

210-48-3

210-48-4

210-49-1
435

SITE 210

0 cm

25

50

75

100

125

150

210-49-2
436

210-49-3

210-50-1

210-50-2

210-50-3

210-50-4

SITE 210

0 cm

— 25
•: :

if

50

75

100

125

150

210-50-5

210-50-6
437

SITE 21000

Velocity (km/sec) and Impedence

Density (gm/cc)
LITHOLOGY

AGE

1.00

1.50

2.00

2.50

4.00

3.00 1.00

UNIT 1LATE
PLEISTOCENE
L.~_" - 50

GRADED CYCLES OF SILT AND CLAY AND
INTERBEDS OF NANNO OOZEApprox. 1900 graded cycles of silt and clay occur
in Unit 1. Most have silt at the base and grade upwards through silty clay and clayey silt to clay at
the top. Colors are various shades of greenish gray,darker at the base. Cycles average 14 cm in thickness.

Approx. 800 interbeds of nanno ooze make up 15%
of Unit 1. Clay content is variable. Relatively clay
free oozes are white, clay rich oozes are darker
shades of greenish gray. Nannofossils are the predominant biogenic component with minor amounts
of foraminifera. The interbeds average 8.5 cm inthickness.

EARLY
PLEISTOCENE

100

11
4,

12

13
-150

14
LATE
PLIOCENE

15

16

-200

17

18
L

250

<D

7.00

10.00

\JΣ£

£7)
13.00

3

SITE 210 cont.
Velocity

Density (gm/cc)

AGE

LITHOLOGY

1.00

Generalized mineralogy for Unit 1:
Graded cycles - mainly subangular quartz andPlagioclase plus mica, calcite and aragonite. Calcareous material is mainly forams in the basal partsof the layers and nannofossils in the upper parts.
Minor constituents include chlorite, altered glass,plant debris, clay minerals, ascidian siderites, amphibole, zeolites, K-feldspar and pyrite.

21
-300

EARLY
PLIOCENE

Interbeds - Mainly nannofossils with varying
amounts of forams, clay minerals and clay sizedparticles.

22

23

350'

LATE
MIOCENE

26-400
27W•-~-

-450

-3or

UNIT 1
UNIT 2AMID
MIOCENE

311

CLAY - semilithified, dark greenish gray, moderately mottled, essentially more calcareous.

32•π_.._L 500

1.50

2.00

2.50

3.00
—I—

— \ UNIT 1 (cont.)

.

1

1.00

4.00

(km/sec) and Impedence
7.00

(^–
10.00

. 2—)
13.00

SITE 210 c o n t .

V e l o c i t y (km/sec) and Impedence

Density (gm/cc)
LITHOLOGY

AGE

j2t-~
Similar to Unit 2A but color is yellowish brown.

f"-£;

MID MIOCENE

Tf

IARLY MIOCENE 3 J |

1.00

1.50

'-as

2.00

2.50

'

4.00

3.00 1.00

7.00

' _

UNIT 2B
UNIT 3EARLY-MID
L~1-.
OLIGOCENE
r-•,- 1 —_ 3 4 l _1_"

CLAY BLARING TO CLAY RICH NANNOCHALK and clay bearing calcic nanno chalk. Yellowish orange to yellow gray.

Λ

©

Λ

©

UNIT 4•LATE EOCENE 3 5 I 1 -•_ _ _ CLAY HI•ARINC TO CLAY RICH CALCIC-bbU NΛNNO CHALK WITH CIII RI NODULKS.

•*

©

^

©

UNIT 5A•f

3 7|fe

CLAY NANNO CHALK, calcic nanno chalk, nanno
clay and calcic clay. Light greenish gray.

"LJfTlT~δB~
As Unit 5A but very pale blue green lo lightgreenish gray, pyrite common in burrows and finally disseminated in bands, sparse forums throughoutwith forum-rich layers below 635 m.

MID EOCENE

4

µU^::

j>

^

-600

©
©

Λ

•
44lF =Hi©

•—' •— — -650

A

®

A

©

A

©

•

46•|—r—~um~ fc

t,

©

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Light bluish gray to light gray, light olive gray filling in burrows, foram bearing throughout with
foram rich layers below 704 m.

EARLY EOCENE 4 ^ r Z 4 Z :
-700
i H—

—

1

4,

•
A

<^ 711 m Bottom of hole^>-

©

0

(

10.00

13.00