3. SITE 212
The Shipboard Scientific Party1

ABSTRACT
Site 212 was drilled in a water depth of 6243 meters in a small
basin of partly ponded sediments in the deepest portion of the
Wharton Basin. Sediment penetration was 521 meters. Fourcalcareous ooze to chalk units, from a few meters to 250 metersin thickness, dominate the stratigraphic section and range in age
from Pliocene to Upper Cretaceous. Each calcareous unit, withthe exception of the late Neogene, one which incorporates aminor hiatus, is of essentially uniform age throughout andcontains residual and in part current-sorted fossil assemblages.
Three nonfossiliferous zeolitic brown clays, averaging 30 meters
thick, separate the calcareous units. The lowermost brown clay
lies directly over a metabasalt which is intercalated with small
quantities of recrystallized carbonate. Observations suggest thatthe brown clays represent normal deep-basin oceanic sedimentation below the carbonate compensation level. The chalk units, on
the other hand, are postulated to be exotic to the area and tohave been transported to the basin by slumping or bottom
current activity from areas of nearby higher elevation. Age ofoldest datable sediment at the site, 34 meters above basalt, isUpper Cretaceous. Age of the recrystallized carbonate in contact
with the basalt is unknown; however, the extrapolated age of
sediment immediately above basalt ranges between extremes of
85 to 110 m.y., depending upon the sedimentation rate chosen
for the brown clay. The basal sediment is unlikely to be older
than Cretaceous and most probably is close to the Early/Late
Cretaceous boundary.

SITE DATA

Date Occupied: 27 Jan 72 (0113)
Date Departed: 1 Feb 72 (1645)
Time on Site: 123 1/2 hours
Position:
Lat 19°11.34'S
Long99°17.84'E
Water Depth (to rig floor):
6240 meters (Echo sounding)6243 meters (Drill pipe)
Penetration: 521 meters
Number of Holes: 1

C. C. von der Borch, Flinders University, Bedford Park, South
Australia; J. G. Sclater, Scripps Institution of Oceanography, La
Jolla, California; S. Gartner, Jr., Rosenstiel School of Marine andAtmospheric Science, University of Miami, Coral Gables, Florida;
R.Hekinian, Centre Oceanologique de Bretagne, Brest, France; D. A.
Johnson, Woods Hole Oceanographic Institution, Woods Hole,
Massachusetts; B. McGowran, University of Adelaide, Adelaide,
South Australia; A. C. Pimm, Scripps Institution of Oceanography;
La Jolla, California; R. W. Thompson, Humboldt State College,
Arcata, California; J. J. Veevers, Macquarie University, North Ryde,
N.S.W., Australia; Lee S. Waterman, Woods Hole Oceanographic Institution, Woods Hole, Massachusetts.

Number of Cores: 39
Total Length of Cored Section: 366 meters
Total Core Recovered: 174.3 meters
Acoustic Basement:
Depth: 516 meters
Nature: Spilitized basalt
Age of Oldest Sediment: Upper Cretaceous
Basement: Spilitized basalt
BACKGROUND AND OBJECTIVES

After drilling Site 211 and obtaining early to middle
Campanian sediments at the base of the section we decided
to drop the alternate site to the north and to head due
south to the deepest part of the Wharton Basin. In theoceans there is a strong correlation between increasing
depth and increasing age of the crust. The purposes of Site
212 are to check the tectonic history of the basin
mentioned in the Introduction and to date the oldest ocean
crust in the Wharton Basin. We chose the deepest.portion of
the basin for Site 212 on the principle that the deepest
crust is also the oldest.
The initial site at 19°ll'S and 99°18'E was selectedfrom a R/V Robert Conrad 9 airgun profile between
Colombo and Freeman tie. The profile showed a thick37

SITE 212

section of greater than 0.4 to 0.5 sec of sediments in a flatbasin, of water 6240 meters deep. This basin is at thesouthern end of a general drop in topography from 5800
meters at 10°S, 100°E to 6250 meters at 19°30'S, 98°E
with rough relief. It is in a zone where the magnetic
anomalies are of low amplitude and is also 500 km to thesoutheast of what was thought to be anomaly sequence 31
through 33. On this evidence it was thought that the age ofbasement would be close to 90 m.y.
A generalized contour chart of the area of the site
(Figure 1) shows that it is located in a flat basin some 40
km long and 20-30 km wide. It is also close, but to the eastof the southern extension of a pronounced north-south
topographic high which may mark an old north-south
fracture zone. The oceanic crust to the east of the high issome 200 meters deeper. Thus, the oceanic crust on which
Site 212 was situated may be slightly older than the cruston which the magnetic anomalies to the north and west arefound. However, the age difference is probably no morethan 10 m.y. A detailed chart of the area of the site has notbeen shown as there was no preliminary site survey.
However, the prominent features in the incoming andoutgoing airgun records can easily be seen on the generalized contour chart (Figure 1 from Carpenter and Ewing,in press). These records are very similar to those of the R/VRobert Conrad. They show that the site was selected in abasin with at least two prominent reflectors within thesediment and no very obvious acoustic or hard rockbasement. Some 0.1 sec of stratified sediments overlie athin transparent layer which in turn overlies alternating
layers of stratified and transparent sediment. Hard rockbasement was estimated at between 450 and 520 meters.
The principal objective at this site was to date basement.
It was expected that the sediment would be predominantly
brown clay. A secondary objective was to sample thissediment extensively for Paleomagnetism and to use themeasurements to determine possible paleolatitudinal shifts
in this portion of the oceanic crust.

deep drilling. Spilitized basaltic basement was reached at a
sediment depth of 516 meters and was cored for 5 meters
to give 4.05 meter recovery.
LITHOLOGIC SUMMARY
Introduction

The sedimentary section penetrated at Site 212 is 516
meters thick; 366 meters were cored with a recovery of 174
meters. The sediments range in age from mid-Pliocene at
the surface to Late Cretaceous (?) 34 meters above basalt.
Basalt was encountered between 516 and 521 meters, atwhich depth the hole was terminated.
Nine lithologic units (Figure 2) are distinguished at thissite as follows:

Unit

Depth
Below Sea
Floor (m)Lithology

1 0 to -30

Interbedded nannoooze and brown clay

2 -30 to 166

Nanno ooze

Nanno ooze andchalk
288.5 to 318.5 Brown zeolitic
claystone
318.5 to 402.5 Nanno chalk402.5 to 430.5 Brown zeolitic
claystone
430.5 to 482.0 Nanno chalk3 166 to 288.545678 482.0-516.0

9 516-521

Brown zeolitic
claystone
Metabasalt withlimestone inclusions

Age

Cores

Mixed Pliocene 1-2
with some late
MioceneMixed late
3-10
Miocene withsome Middle
Miocene
Early middle
10-14
Miocene
9
15-18
Mid-Eocene
?

18-27
27-29

Late
Cretaceous

29-35

?

35-38
39

OPERATIONS

Site 212 was approached along a course of 164° in orderto run in on a seismic profile collected by R/V RobertConrad. The site was selected in a deep basin containing
ponded sediments, approximately 40 nautical miles inextent along the seismic line of Conrad 9. A spar buoy was
dropped overboard at the chosen site and the seismic gear
secured, after which a Williamson Turn was made toapproach the drilling locality. The beacon was dropped in awater depth of 6243 meters. This represents the deepest
site occupied by Glomar Challenger to date.
Coring was planned on the basis of one core every 20 to
30 meters to within 100 meters of basement, with
continuous coring of basal sediments to basement. The bit
used was a Smith 93 CJS. A total of 39 cores was
ultimately recovered with an overall recovery of 47.6%(Table 1).
No drilling or coring difficulties were encountered at thissite, despite the fact that the longest drill string (6764
meters) to be suspended from a floating drilling vessel was
employed. Hole condition in the stiff brown clays andnannofossil chalks, as well as the weather, were ideal for

38

Description
Unit I-Interbedded Nannofossil Ooze and Brown Clay(Cores 1, 2)
An interbedded sequence of foraminifera-bearing nannofossil oozes and brown clays constitutes Unit 1. About 90%
to 95% of the grayish orange oozes consist of calcareous
nannofossils; foraminifera generally constitute less than 5%
and decrease in abundance toward the base of the section.
The brown clays contain a few percentage of nannofossils
but consist principally of clay minerals and iron-oxide-richclay aggregates. Pockets containing up to 75% of volcanic
glass occur in the clay at a depth of 10 meters. Between
12.5 and 14.5 meters (Core 2), clay and ooze alternate inbeds only 5 to 10 cm in thickness. Generally, the ooze overclay contacts are sharp, whereas clay over ooze contacts aregradational and characterized by lithologic mottling.
The lower boundary of this unit was picked arbitrarily at
a depth midway between Cores 2 and 3—a vertical distanceof 23 meters.

SITE 212\ • \ \ / 7

V
5

v

5.5

v

5.'

105°
Figure 1. Location of Site 212.

Units 2, 3—Nannofossil Ooze and Chalk with
Minor Brown Clay (Cores 3-15)
The difference between Units 2 and 3 is defined by age
on the basis of the nannoplankton floras (see later), theirlithologies being essentially similar. Unit 2 consists offine-grained nannofossil ooze, but Unit 3 is mostly chalk
becoming lithified at a depth of about 220 meters. The
color changes gradually from very pale orange at the top toyellowish gray below, this trend being accompanied by anincrease in clay content from 2% to 3% near the top to 25%
to 20% in the lower part (confirmed by CaCC»3 analysis).
Generally whole and fragmental foraminifera constituteonly 1% to 2% of the total sediment; however, three zones
of relative foraminifera enrichment are evident: between 60
and 70 meters where foraminifera range from 2% to 8%,
between 250 and 262 meters, and between 288 and 288.2
meters where foraminifera make up about 40% to 50%,thus constituting nannofossil-foraminifera chalk. The
foraminifera-rich zones contain less clay, and in the lower,
more prominent zones, coarse silt-sized feldspar, rockfragments, and heavy minerals are present. All foraminiferarich zones are laminated; however, lamination is bestdeveloped in Core 13 (250.0-259.5 meters) where thevariety of sedimentary structures present include: (1)Well-developed horizontal lamination (alternating light anddark layers); (2) Rare cross-lamination; (3) Contorted
lamination, some of which appears as small-scale flute orload casts. The lowermost nannofossil-foraminifera chalk
immediately overlying Unit 3, appears graded and contains
fragments of green claystone along with a trace ofglauconite (Core 15).
Units 4, 6, 8—Brown Zeolitic Claystone(Cores 15-18, 27-29, 35-38)
Although these zeolitic claystone units vary from one
another in detail, the number of lithologic similarities
justifies considering them together. Each unit is on theorder of 30 meters thick and encased either between chalklayers or, in the case of Unit 8, between chalk and basalt.
The prevailing colors are moderate brown, dusky brown, or
dusky yellowish brown. These colors often occur mottled
together or as alternating bands, though in each case a partof the unit is uniformly dark brown and apparently
manganese rich. Near the top of each unit occurs a layer ofgreenish to bluish gray claystone ranging from 5 to 30 cm
in thickness. In Units 4 and 8 this layer occurs at thecontact with the overlying chalk; in Unit 6 it is separated
from the chalk by 40 cm of brown claystone.

39

SITE 212
TABLE 1
Coring Summary, Site 212

Date
(Jan/
Depth from
Depth Below Length Recovered Recovery
Core Feb) Time Drill Floor (m) Sea Floor (m) Cored (m)
(m)
(%)
1
2
3
4
5
6
7
8
9
10
11
12
13
14
15
16
17
18
19
20
21
22
23
24
25
26
27
28
29
30
31
32
33
34
35
36
37
38
39

28
28
28
28
28
28
28
28
28
28
29
29
29
29
29
29
29
29
29
29
30
30
30
30
30
30
30
30
30
30
31
31
31
31
31
31
31
31
1
Feb.

0305 6243.0 6252.5
0-9.50515 6252.5-6262.0
9.5-18.00735 6284.0-6293.5
41.0-50.5
0940 6293.5-6303.0 .30.5-60.01155 6303.0-6312.5
60.0-69.5
1400 6331.5-6341.0
88.5-98.0
1550 6350.5-6360.0 107.5-117.0
1805 6369.5-6379.0 126.5-136.0
2015 6379.0-6388.5 136.0-145.5
2245 6407.5-6417.0 164.5-174.00150 6436.0-6445.5 193.0-202.50505 6464.5-6474.0 221.5-231.00755 6493.0-6502.5 250.0-259.5
1015 6512.0-6521.5 269.0-278.5
1315 6531.0-6540.5 288.0-297.5
1530 6540.5-6550.0 297.5-307.01730 6550.0-6559.5 307.5-316.5
1935 6559.5-6569.0 316.5-326.0
2130 6569.0-6578.5 326.0-335.5
2335 6578.5-6588.0 335.5-345.00145 6588.0-6597.5 345.0-354.5
0340 6597.5-6607.0 354.5-364.00550 6607.0-6616.5 364.0-373.5
0845 6616.5-6626.0 373.5-383.0
1040 6626.0-6635.5 383.0-392.5
1230 6635.5-6645.0 392.5-402.0
1420 6645.0-6654.5 402.0-411.5
1615 6654.5-6664.0 411.5-421.0
2030 6664.0-6623.5 421.0-430.S
2315 6673.5-6683.0 430.5-440.00145 6683.0-6692.5 440.0-449.50425 6692.5-6702.0 449.5-459.0
0710 6702.0-6711.5 459.0-468.5
1015 6711.5-6721.0 468.5-478.01200 6721.0-6730.5 478.0-387.5
1515 6703.5-6740.0 487 5-497.0
1750 6740.0-6749.5 497.0-506.5
2030 6749.5-6759.0 506.5-516.00040 6759.0-6764.0 516.0-521.0

Total

9.5
9.5
9.5
9.5
9.5
9.5
9.5
9.5
9.5
9.5
9.5
9.5
9.5
9.5
9.5
9.5
9.5
9.5
9.5
9.5
9.5
9.5
9.5
9.5
9.5
9.5
9.5
9.5
9.5
9.5
9.5
9.5
9.5
9.5
9.5
9.5
9.5
9.5
5.0

9.5
7.5
0.8
1.5
1.9
0.2
1.5
5.5
0.7
9.0
4.6
6.5
4.7
8.0
4.1
2.7
0.5
3.6
1.9
0.9
6.0
4.7
6.7
0.5
9.5
9.5
6.2
4.5
1.6
3.4
8.6
9.2
9.2
3.3
6.7
1.0
1.4
2.1
4.0

100
80
8
17
20
2
17
60
7
100
48
67
50
84
45
33
6
40
20
9
63
49
70
5
100
100
65
50
20
37
90
97
97
34
70
10
16
23
80

366.0

173.7

47.6

Note: Echo sounding depth (to drill floor) 6240 meters;
drill pipe length to bottom = 6243 meters.
Compositionally these units range from zeolite-bearingiron-oxide-rich claystone to clay zeolitites (>50% zeolite).
Other persistent constituents, usually in concentrations ofless than 5%, include: opaques (Mn micronodules), volcanic
glass, and a significant fraction of very fine (<4µ) iron-40

oxide spherules (probably goethite) and equally fine, highrelief, nonopaque grains of heavy minerals. The content ofzeolite and the degree of crystalinity generally increase withdepth within each unit; however, these are not uniform
trends.

SITE 212
SITE 212

Nanno Ooze
Brown Clay

-100

Nanno Ooze

-166

12

Nanno Chalk

318.5

anno Chalk

3EC-1
eolitic
lay
430.5

anno Chalkeolitic
lay516

Figure 2. Lithologic units at Site 212.
One prominent feature which differentiates the claystones of Units 6 and 8 from Unit 4 is the occurrence ofthin bands (< 10 cm) of pale olive claystone surrounded by"halos" of reddish brown, iron-oxide-enriched claystones.
These are best developed in Core 28 (see core photos andcore summary log).

Unit 5-Nannofossil Chalk (Cores 18-27)
Fairly uniform nannofossil chalk comprises the bulk of
Unit 5. From examination of smear slides onboard the ship,
the CaC03 content was estimated at more than 90%, but
the CaCOß analyses show it to be closer to 80%. The unit
ranges in color from white near the top to light gray or
pinkish gray at the base. A trace of siliceous micro fossils(rads, sponge spicules, and diatoms) is evident in the upper
chalk. The siliceous component increases to a maximum of
about 12% at a depth of 347 meters (Core 21) and tails off
again to trace amounts in the lower part of the unit. Micarb(see Explanatory Notes, Chapter 1) ranges between 1% and
5%, and a trace (< 1%) of glauconite persists throughout theunit.
A green, zeolite-rich claystone bed (20 cm thick) occurs
in Core 23. Immediately above and below this bed, thechalk is conspicuously laminated and contains fragments ofgreen claystone.
Unit 7-Nannofossil Chalk (Cores 29-35)
Clay-bearing to essentially pure (>95% nannofossils)
nannofossil chalk constitutes the bulk of Unit 7. This unit
varies in color from grayish orange pink in the upper 13 to
14 meters to light olive gray with abundant mottles ofgreenish gray in the lower part. Volcanic glass andmanganese micronodules comprise a significant admixture
to the nannofossils in the upper 2 to 3 meters of the unit.
Small whole foraminifera and foraminiferal fragments
gradually increase from about 1% to 2% in the upper
section to a maximum of 30% in the lower 3 meters, thus
yielding a gross textural grading to the unit. This increase isaccompanied by color banding (lamination?) and thepresence of fragments of green claystone similar to that
immediately underlying this unit. Micarb and recrystallized
foraminifera increase from a few percent in the upper
section to 10% near the base.
Unit 9—Basalt with Recrystallized Limestone(Core 39)
Unit 9 consists of partially weathered, altered basalt
with altered drilled margins of chlorite bearing basaltic glass(< 10 cm thick).
The inner part of the metabasalt is phaneritic containing
phenocrysts and microphenocrysts of partially altered
Plagioclase set into a medium coarse-grained matrix having
intersertal texture. The interstices between the altered
Plagioclase laths are filled with chlorite, pyroxene granules,
dark brown mesostasis, and calcite. Chlorite, calcite,
pumpellyite, and occasional epidote are often included inboth the Plagioclase microphenocryts and the matrix
Plagioclase.
The metabasalt changes its textural features near thebasaltic glassy zone becoming phaneritic with a finergrained and more cryptocrystalline matrix. This finergrained metabasalt zone is also more weathered and grades
into a chloritized glassy zone.
The chloritized glassy zone consists of palagonite, brownglass, and chloritic aggregates and smectite. At least sevendifferent chilled margins with gradual grain-size and textural variations were noticed within the recovered core.

41

SITE 212

These variations suggest the occurrence of pillowed structure. Trapped between the pillow lavas there are somelimestone fragments consisting almost entirely of recrystallized calcite and very little Plagioclase. In places near thecontact of the rock unit, angular fragments of chloritized
glass and fragments of crystalline metabasalt are incorporated in the carbonate rocks. Traces of fossils were
noticed. The content of trapped limestone material
decreases with depth in the core.
Discussion

The most conspicuous problem in interpretation of thesedimentary section at this site pertains to the reason (orreasons) for alternation of calcium-carbonate-rich andnoncalcareous sediments. At least two plausible interpretations are obvious: (1) the calcium carbonate compensation
depth has fluctuated repeatedly relative to the bottom
depth at this site; and (2) the site has remained continuously below the CaCC 3 compensation depth, but
carbonate sediments were flushed in rapidly from shallower
water on several occasions and thus preserved.
Several features of the recovered sediments which bearon this problem and seem to favor the second interpretation include the following:1) The similarity of the claystone units at various levels
within the section.
2) Presence of occasional coarser foraminifera-richlayers which grade upward into finer nannofossil chalks.
Relatively coarse terrigenous material accompanies theforaminifera-rich layers in at least one case.
3) Lamination and cross-lamination in the foraminiferarich zones indicative of substantial bottom current activity.
4) In all cases where chalk is observed overlying
claystone the contact is sharp. In contrast, in two
observable cases, clay over chalk contacts are diffuse andgradational, arguing for gradual return from somewhat
catastrophic carbonate depositing intervals to morequiescent clay accumulation. Concentration of manganeseand clay in the upper part of the Cretaceous chalk suggests
a gradual slowing of carbonate deposition, though theactual contact with overlying clay was not observed.
5) Incorporation of claystone clasts in the chalks
immediately above the contact zones.
6) Persistent (though minute) fraction of glauconite
throughout the chalk of Lithologic Unit 4 and in the lower
foraminifera nannofossil chalk of Lithologic Unit 2.
7) Small-scale interbedding of brown clay and ooze
which is incompatible with a slowly fluctuating process
such as a change in compensation depth.
CHEMICAL PROPERTIES

Twenty-three cores were sampled at this site, and a listof the results obtained is given in Table 2. Insofar as waspractical, minicores or generous portions from the corecatcher material were taken from every core when spot
coring and from alternate cores when continuously coring.
Principal lithologic units were sampled whenever theyoccurred.
All samples were warmed to ambient room temperature
prior to making punch-in pH and resistivity measurements.
Punch-in pH measurements were made on only three

42

TABLE 2
Shipboard Chemistry ResultsCore,
Section,Interval
(cm)

Water

Porosity

Density(gm/cc)

38
57
58
53

64
80
86
79

1.68
1.40
1.48
1.50

-

-

-

31
27

59
48

29

56

1.87
1.77
1.89

pH

2-1,422-1,1102-3,06.9
2-3, 109
5, CC
7.4
8-3,0
8-3, 2
9-1,110
10-1, 30
10-4, 100
10-5,07.4
10-6, 100
11-1, 144
11-3,0
6.9
11-4, 143
12-1, 14112-4, 06.9
13-2, 7
13-2, 15
13-3, 06.9
14-5, 06.8
15-2,11
15-3, 07.0
16-1, 150
16-2, 06.9
18-2, 81
18-3, 140 7.2
20, CC 6.7
20-1, 126
21-3, 06.9
22-2, 139
22-3, 06.8
23-1, 83
23-3, 0
6.9
25-5, 0
6.7
27-4, 16
7.0
27-5, 028-1, 34
29, CC
6.7
29-1, 64
31-1, 102
31-5, 07.0
33-2, 68
6.5
33-3, 035-2,06.8
36-1, 108 36-6, 46
6.8
37, CC
37-1, 43
38-2, 32
-

25
26
25
26
15
25
23
22
23
32
29
32

49
45
29

1.95
1.71
1.91

-

(darker material)(lighter material)

21

-

-

35
41
31
32

54

1.58

-

-

32

38

1.19

27
27

-

-

25

-

-

26
25

-

-

25

-

-

15

—

-

31
30

53

1.72

28

-

-

16
29

52

1.80

17

-

-

10
13

-

-

14

—

-

26

-

-

27

:

31

-

-

samples at the top of the hole owing to the stiffness of theclays and impenetrability of the chalks. Direct readings ofresistivity was attempted on all of the minicores and some

SITE 212

large pieces taken from the core catcher. This procedure
was successful on the hard sediments only when it waspossible to drill holes for inserting the electrodes withoutcausing the material to break into pieces.
Samples from the top of the hole were squeezed toobtain pore fluids as soon as practical after warming toroom temperature. Later, chalk samples were held forincreasingly longer periods before squeezing was started
owing to the difficulty in getting pore water out of thesedrier and harder sediments. All the chalks were squeezed in
the 4.25-cm Manheim squeezer, and multiple squeezings
were necessary in all cases. The driest material encountered
was in Sample 18-3, 140-150 cm, which was squeezed in six
portions and yielded only 6.8 ml of pore fluid. In nearly all
instances, pore water recovered from an individual portionof sediment represented the amount which could be
extracted in a maximum of 10 min of applying pressure. In
most instances a total of 10 to 12 ml of interstitial water
was obtained.
The pH values of the pore water measured with theflow-through electrode reach a maximum of 7.41 in theCore 10 sample (~ 170 meters) and a minimum of 6.54 inCore 31 (-460 meters). Between Cores 11 (193 meters)and 37 (506 meters) the pH averages out to 6.86 with themost notable departures occurring in Cores 18 and 31. The
somewhat regular alternation of plus and minus deviations
from the average, a "sawtooth" effect, seen in this profile
may be partly attributable to sample handling, particularly
the necessity for multiple squeezings and prolonged squeezing time.
Pore water salinities, estimated with a Goldberg refractometer, show only small departures from ocean water
values and are more or less randomly scattered between
34.4 °/oo and 36.3 % o .
BIOSTRATIGRAPHIC SUMMARY
GeneralThe sediments recovered at Site 212 yielded calcareous
as well as siliceous fossils in some parts of the section.
Planktonic foraminifera were recovered in Cores 1 through15, but for the most part these are small forms ill suited forbiostratigraphy. Useful Miocene assemblages were recoveredin Cores 6, 7, 10, 11, 13, and 15. Below Core 15 noforaminifera were recovered down to Core 29, except forsome few small planktonics in Core 23, which, however, are
not useful. Cores 29 through 36 yielded a rich assemblageof very small specimens, including unusually large numbersof heterohelicids.
Coccoliths and associated calcareous nannofossils arepresent in profusion where the sediment is calcareous. They
are, for the most part, useful for dating the sediments,
although in several instances only broad age assignments are
possible. A marked lack of species diversity is apparent
from Core 10 on down, and this also coincides with poor
preservation and fragmentation of most of the nannofossils.
It is inferred that solution has removed all but the mostresistant species from the assemblage, and that which
remains may be termed properly a residual thanatocoenose.
Radiolaria are sparsely represented in Cores 1 and 3 andindicate a late Neogene age, in agreement with thecalcareous fossils with which they occur. A broader
assemblage is present in Cores 19 through 23 and indicatesan early middle Eocene age. As the associated nannofossils
indicate a slightly younger age, it is likely that theRadiolaria have been redeposited.
Foraminifera

Cores 1 to 4 inclusive contain numerous minute globigerinids and globorotaliids; these are abundant in Core 5
together with fragments of larger tests. Cores 6 to 12 are
the same, although some useful larger specimens wererecovered from Cores 6, 7, 10, and 11. The occurrence ofabundant tiny planktonics over this interval would seem toindicate rather consistent size fractionation during someprocess of redeposition. There are also some indications of
mixing: species expected to have nonoverlapping ranges arefound together.
Globorotalia conomiozea in Cores 6 and 7 indicate ahigh upper Miocene age (N.I7 or higher), although thespecies seem to occur also (more rarely) in Cores 10 and 11.
G. siakensis and G. cf. peripheroronda are evidence for amixing-in from older assemblages. Core 13 is different fromthe others as it contains a foraminiferal sand; again, mixing
is suggested by the association of Oligocene species {Globorotalia opima, Globigerina prasaepis) with middle Miocene(Globigerina nepenthes; N.I4 or younger).
The dominant globorotaliids are Globorotalia conomiozea (in the upper Miocene) and G. miozea with its
variant conoidea. These forms are well known in New
Zealand and this, together with the virtual absence oftypical tropical globorotaliids and other genera, suggeststhat the middle and upper Miocene feeding the section at
Site 212 was "extratropical" in character, i.e., closer in its
appearance to assemblages from New Zealand and southern
Australia, and unlike the Miocene known from lower
latitudes.
Core 15 contains a poor fauna which seems probably to
be in situ. Single specimens of a few species indicate a lower
Miocene age.
Cores 29 (lower calcareous part) to 35 contain a very
distinctive foraminiferal assemblage characterized by: (1)minute size, all passing through the 100-mesh sieve (150µ);(2) abundance of planktonics, some calcareous benthonics;(3) no biostratigraphic change through the section; (4)seemingly no juvenile Globotruncana or other forms characterizing assemblages from warmer water masses; and (5) adistinctly greater proportion of biserial tests of heterohelicids than would be expected in a "normal open marine"
planktonic foraminiferal assemblage.
As in the Miocene, the restricted size range indicatesmechanical fractionation during redeposition. However, no
mixing of different faunas is discerned (the common forms
are long ranging). The apparent absence of Globotruncana
suggests perhaps that the original deep-water assemblage
was extratropical. Selective solution would explain neither
the taxonomic bias nor the size bias. The abundance ofheterohelicids is unexplained; Pessagno (1969) has suggested that they might indeed be less common in abyssal
pelagic deposits, but the evidence of Douglas (1971) does
not support this.

43

SITE 212

The agglutinated assemblage in Core 36 is of deep-waterorigin. It is quite different in overall character from theassemblage in the Upper Cretaceous at Site 211.
A specimen in a thin section from Core 39 (Section 1,
143 cm) is of a calcareous-perforate foraminifera, quitepossibly a buliminid. A Cretaceous (rather than Jurassic)
age is quite likely.
Nannofossils

Calcareous ooze or chalk rich in nannofossils constitutes
the bulk of the sediment recovered at Site 212. The age ofthe calcareous sediments ranges from late Neogene to Late
Cretaceous, the latter being separated from basement byseveral meters of red clay.
On the basis of calcareous nannofossils, the section
penetrated at this site can be divided into several distinct
units. Three of these units are brown clay devoid of
nannofossils; five units are calcareous ooze or chalk. The
lowermost unit consists of basalt and recrystallized limestone without identifiable fossils. From top to bottom theeight upper units have the following position and age
relationships.
Unit 1 (Cores 1 and 2): mixed Pliocene calcareous ooze
interbedded with brown clay in Core 2 and containing somelate Miocene and mid-Tertiary contaminants.
Unit 2 (Core 3 to Core 10, Section 2): mixed late
Miocene calcareous ooze with some middle Miocene andmid-Tertiary contaminants.
Unit 3 (Core 10, Section 2 through Core 15, Section 1):
early middle Miocene chalk (Sphenolithus heteromorphus
Zone) with sparse but consistent Eocene-Oligocene contaminants. No significant age difference seems discernible
from the top to the bottom of this thick chalk. The span is
17 to 15m.y.
Unit 4 (Core 15, Section 1 through Core 18, Section 2):
brown clay barren of nannofossils.
Unit 5 (Core 18, Section 3 through Core 27, Section 1):
middle Eocene chalk. The age of this chalk is within thetime interval of the earliest occurrence of Reticulofenestra
umbilica about 47 m.y. and the last occurrence ofChiasmolithus grandis about 43 m.y.
Unit 6 (Core 27, Section 1 through Core 29): brown
clay barren of nannofossils.
Unit 7 (Core 30, CC through Core 35): Upper Cretaceous
chalk. This last unit is an enigma as to precise age. It
consists almost exclusively of long-ranging Upper Cretaceous species which indicate Santonian or younger age.
Sporadically throughout this unit Nephrolithus frequens is
encountered, however, and this species indicates a late
Maastrichtian age.
Unit 8 (Core 36 through Core 38): brown clay barren of
nannofossils.
Units 1 and 2 contain moderately diverse oceanic
assemblages of nannofossils with about the normal numberof species present and the specimens, for the most part, arewell preserved. The mixed nature of the nannofossil
assemblages in these two units suggests that both wereredeposited probably from a turbidity current.
The Unit 3 assemblage is dominated by one species,
Cyclicargolithus floridanus, and much of the calcareousmaterial consists of unidentifiable fragments of coccoliths

44

and other nannofossils. The marker species Sphenolithus
heteromorphus, though rare, is consistently found in thischalk. In addition, several Eocene-Oligocene species arefound throughout Unit 3, indicating that some transportand redeposition occurred in the region at this time.
Units 5 and 7 are in overall aspect similar to Unit 3 inthat the assemblages are dominated by a relatively small
number of species, and much of the calcareous material
consists of fragmented nannofossils. This paucity of species
in these last two units is even more notable as the intervals
they represent (middle Eocene and Upper Cretaceous,respectively) elsewhere yield some of the most diverse
assemblages known. It seems reasonable, therefore, thatmany species have been removed through selective solution,and only the more resistant have been preserved. Units 5
and 7 differ from Unit 3 in one significant aspect: they
contain no older redeposited species.
It is also noteworthy that although Units 1, 2, 3, 5, and7 consist of substantial thicknesses of chalk and calcareous
ooze, they represent relatively short periods of time. The
total time represented by calcareous sediment is perhaps
not more than 15 m.y., although the section cored ranged
over a 70-m.y. interval.
Radiolaria
At Site 212 poorly preserved Radiolaria are present in
the core-catcher samples of Cores 1 and 3. Radiolaria areabsent between the bottom of Core 4 and Core 19, Section
2. Moderately preserved to well-preserved Radiolaria of
middle Eocene age are present between the bottom of Core19 and Core 23, Section 3. Radiolaria are absent in theinterval between Core 23, Section 5 and the volcanic rockencountered at the bottom of the hole.
The sediment in Cores 1 and 3 contains poorly preserved
fragments of Radiolaria, including Ommatartus tetrathalamus, Euchitonia elegans, Lithopera bacca, andTheocorythium trachelium. A late Miocene to Pliocene age
is assigned on the basis of the nannofossil assemblagespresent in these cores.
A portion of the middle Eocene chalk unit, between thebottom of Core 19 and Core 23, Section 3, contains awell-preserved assemblage of diatoms and radiolarians. The
radiolarian assemblage includes common specimens ofLophocyrtis biaurita and rare to common occurrences ofPhormocyrtis striata striata, Theocotyle cryptocephalacryptocephala, Lamptonium fabaeforme fabaeforme, and
Lychnocanoma babylonis. Theocampe mongolfieri is present in trace amounts, whereas the form which is believed
to be its precursor {Theocampe amphora) is much morecommon. The age of the radiolarian assemblage in thesecores appears to be lowermost middle Eocene, probably
near the base of the Theocampe mongolfieri Zone.
However, the nannofossil assemblages within this part ofthe core suggest a slightly younger age, probably upper
middle Eocene (see section on nannofossils).
CORRELATION OF REFLECTION PROFILEAND STRATIGRAPHIC COLUMN

The seismic reflection profile over Site 212 (Figure 3)
shows an upper acoustically transparent zone about 0.16
sec in thickness, largely obscured by the bubble pulse. This

SITE 212

meters_CaJ careous _ooze_ _Calcareous ooze and brown clay

SITE 212

Calcareous ooze

Chalk
Reflector 1
Brown clay

Reflector

Chalk

Brown clay

Chalk

Brown clay

500-

BasaltFigure 3. Correlation of reflection profile and stratigraphic column at Site 212.

45

SITE 212

is underlain by a well-defined zone of reflections 0.08 sec inthickness which is herein termed Reflector 1. Below
Reflector 1 lies Reflector 2, at 0.35 sec. Acoustic basement
at this site is difficult to define on the seismic profile.
However, by extrapolation a highly irregular zone below
the lowest coherent reflectors suggests seismic basement to
be at a depth of about 0.45 sec.
An overall view of the seismic record suggests that alllayers above Reflector 1 are essentially horizontally disposed, while the upper surface of Reflector 1 and all layers
below appear to be draped over the rough basement
topography possibly due to sediment compaction.
Although no definite conclusions are possible, the most
likely correlation between the stratigraphic column andairgun seismic reflection profile is illustrated in Figure 3.
The whole zone down to the top of Reflector 2 may
correspond with the Pliocene to middle Eocene nannofossil
ooze, nannofossil chalk, and clay. This unit, 403 meters
thick, is represented by 0.35-sec two-way travel time on theseismic profile, giving it an interval velocity of 2.3 km/sec.
Lithological variations within this zone, apart from the clay
interbeds, are extremely small. Reflector 1 possibly correlates with a bed of stiff clay, and Reflector 2 with the topof a bed of clay at 403 meters.
Below Reflector 2 no definite correlations can be madedown to acoustic basement at about 0.45 sec. The thicknessof 113 meters of sediment between the zone correlatedwith Reflector 2 and basaltic basement in the column,
corresponding to 0.10-sec two-way time on the seismic
record, gives an interval velocity of 2.3 km/sec for the
lower sedimentary unit, a velocity which agrees with theobserved semi-indurated nature of these sediments.
Depths of reflectors and interval velocities are as
follows:
Reflector

2-Way Time (sec)

Depth
(m)

0
0.16
0.35
0.45

0
170
403
516

Interval Velocity(km/sec)
2.1
2.5
2.3

2.3

SUMMARY AND CONCLUSIONS

Site 212 is situated in the deepest portion of the
Wharton Basin in a water depth of 6233 meters. The site
locality lies within a sedimentary basin about 35 km in
length in an area of rough outcropping basement near thesouthern termination of the approximately north-south
trending Investigator Fracture Zone (Sclater and Fisher, in
preparation). The region on either side of the fracture is amagnetically quiet zone coinciding with the Wharton Basin.
The seismic reflection profile over the site made by Glomar
Challenger (see Chapter 10) suggests ponding of uppermost
sediments in the basin and compaction draping of deeper
and older sediments over basement topography.
The deepest lithologic unit cored, which may represent
oceanic basement, consists of a succession of altered andweathered pillow lavas termed metabasalts. These haveapparently suffered hydrothermal alteration, possibly due

46

to the proximity of the Investigator Fracture Zone mentioned above. Minor intercalcations of recrystallized carbonate between pillows represent older sediments trapped
during the emplacement of the basalts. These rocks have all
the characteristics of weathered mid-Indian Ocean Ridge
basalts.
The sedimentary column overlying the metabasalt contains seven lithostratigraphic units comprising four calcareous oozes grading to chalks, 30 to 250 meters thick,alternating with three zeolitic brown clay units averaging 30
meters in thickness, the lowermost of which lies directly on
the metabasalt.
Ages of the calcareous units have been determined
paleontologically as early-late Pliocene to late Miocene,
early middle Miocene, middle Eocene, and Maastrichtian.
Sedimentological and biostratigraphic evidence (thischapter and Chapter 39) implies an exotic source for thecalcareous units and suggest the sediments were emplaced
by a combination of turbidite and nepheloid layer transport.
Historic periods of significant carbonate accumulation
which were related to concomitant and episodic lowering of
the carbonate compensation depth are documented in theoceans (Chapters 39 and 41). Each lowering was associatedwith carbonate accumulation on highs. The exotic chalkunits at Site 212, which are postulated to have beentransported to the locality are tentatively correlated withthese episodes.
Estimate of Basement Age

The lithology of Site 212 consists of four sections ofbrown clay separated by three sections of nannofossil ooze
grading to nannofossil chalk. The fourth brown clay section lies directly above basement which is metabasalt
containing minor interbedded crystallized calcareous sediments. Unfortunately, there are no fossils in the brown clay
and no datable fossils in the crystallized calcareous sediment, thus an exact age cannot be given to the basementsediment contact. However, a rough estimate can be madeif the sedimentation rate of the bottom brown clay can be
determined.
The lithology of the site appears to represent continuous
slow deposition of brown clay sediment interrupted byshort pulses of much more rapidly deposited calcareousunits. If the brown clay sedimentation rate is assumed
uniform to a first approximation, then the age of the top
and bottom of each clay section is given by the youngest
age of the calcareous sediment immediately above andbelow. From such ages an average sedimentation rate of 0.7
to 1.6 m/m.y. can be computed for the two clay sections.
The general uniformity of rates for the two sections and thesimilarity to rates in the Pacific support the assumption of a
uniform rate of brown clay sedimentation. As the lowermost brown clay section differs little from those above it,
the sedimentation rate can be used to estimate an age forthe brown clay metabasalt contact. Assuming a 65 to 72
m.y. age span for the Maastrichtian and a thickness of 34
meters for the basal brown clay section, the contact age
ranges from 85 to 110 m.y. with a mean value of close to
100 m.y., assuming an average sedimentation rate of 1

SITE 212

m/m.y. Thus the best age estimate lies close to the
Early/Late Cretaceous boundary.
Site 212 is located at the southern extremity of theInvestigator Fracture Zone. As it is not obvious on whichside of this north-south trending fracture the site is located,
it cannot be used quantitatively to aid tectonic reconstructions. On the other hand, this site does show (a) that theage of the oceanic crust in the central Wharton Basinincreases to the south and (b) the central Wharton Basin is
no older than Cretaceous.

Douglas, R. A., 1971. Cretaceous foraminifera from theNortheastern Pacific Ocean: Leg VI, Deep Sea Drilling
Project. In Fischer, A. G. et al. Initial Reports of the
Deep Sea Drilling Project, Volume VI: Washington (U. S.
Government Printing Office), p. 1027-1053.
Pessagno, E. A., 1969. Mesozoic planktonic foraminifera
and Radiolaria Leg I, Deep Sea Drilling Project. In
Ewing, M. et al. Initial Reports of the Deep Sea Drilling
Project, Volume I: Washington (U.S. Government
Printing Office), p. 607-621.

REFERENCES
Carpenter, G. and Ewing, J., in press. Crustal deformationin the Wharton Basin: J. Geophys. Res.

Sclater, J. G. and Fisher, R. L., in preparation. The
evolution of the East Central Indian Ocean withemphasis on tectonic setting of Ninety east Ridge.

47Site 212

Hole

Core 1

Cored Interval: 0-9.5 m

S i t e 212

HoleCore 2

Cored I n t e r v a l : 9.5-18.0 m

LITHOLOGIC DESCRIPTION

LITHOLOGIC DESCRIPTIONa θ i norkPt<:
asn pockets

NANNO OOZE
grayish orange (10YR7/4)
f a i n t laminations o f enriched
i r o n oxide
Volcanic glass
75%
Undiff. clay
20%
Other volcanogenic
minerals, chiefly
feldspar and hornblende
5%
IRON OXIDE BEARING CLAY
moderate brown (5YR3/4) withmottles of grayish orange(10YR7/4).
Contains pockets of r h y o l i t i c
ash and from 2-5% s i l t .
General composition:
Clay
88-96%
Iron oxide aggregates 2-10%
Zeoli tei%

NANNO OOZE
grayish orange (10YR7/4)
general composition:
Nannofossils
80-85%
Forams4-8%Volcanic ash
1 - 1%
I r o n - c l a y aggregates
1- 2%
ZeolitesTr.

gradational

soupy and disturbed

gradational

Interbedded:
CLAY, moderate brown (5YR3/4)
NANNO OOZE, grayish orange(10YR7/4)
Contacts between beds generally
sharp with exception of two
indicated which show gradualtransition from ooze upward
into clay.
General composition:
CLAY LAYERS
Clay
92%
Nannos4%
Iron oxide andaggregates
4%
NANNO OOZE LAYERS
Nannos
77-99%
Clay
1-20%
Forams0- 3%both l i t h o l o g i e s contain up to
15% terrigenous<?) s i l t c h i e f l y feldspar

X-ray a t 10.70 m Quar 35, Feld 5, Plag 7, Kaol 21,
Mica 2 1 , Mont 11

Site 212

Hole

R
A
R

P
G
M

Core
CatcherCore 4

Mi
J_

1
1

I36

J_J.

i±±±i

NANNO OOZEVERY PALE ORANGE (10YR8/2)
f a i n t lamination - 110-120 cm,
130-140 cm
Composition:
Nannos
96%
Clay
3%
Mica
1%
Core contains abundant r u s t
from d r i l l s t r i n g !

N

A

1

1
1
1
1
1
1

LITHOLOGIC DESCRIPTION

21
25
NANNO OOZE,
very pale orange (10YR8/2)
Composition:
Nannos92-93%
Forams2- 8%Volcanic glass
Tr.
ZeoliteTr.
many o f forams are fragmented

il•^-L-•--L-- 1

•°~

R
N
F

DEFORMATION

LITHOLOGY

0.5-

G

LITHO.SAMPLE

Cored I n t e r v a l : 6 0 . 0 - 6 9 . 5 m

METERSPRES.

SECTION

Core 5

ABUND.

FOSSIL

ZONE
Mixed assemblage

1

LITHOLOGIC DESCRIPTIONAGE

DEFORMATION |
I
1
1

Hole
FOSSILCHARACTERLATE MIOCENE

÷-Z±Z•LITHO.SAMPLE |METERSO—i

1

LITHOLOGY

1 1 1 1 1 1 1 1 1 1 1 1 1

PRES.

ABUND.

FOSSIL

ZONE
Mixed assemblage

LATE MIOCENE

AGE

FOSSILCHARACTERF
NR

S i t e 212

Cored I n t e r v a l : 4 1 . 0 - 5 0 . 5 m

Hole

SECTIONS i t e 212

1

A
C

G
F

Core
Catcher

Cored Interval:50.5-60.0 m
Subtle lamination a t scale of2-3 mm; r e f l e c t s differences
i n foram content.

LITHOLOGIC DESCRIPTIONGF

LITHOLOGYCore
Catcher

NANNO OOZE

Cored In terval : 07. 5-117.0 m

Core 7l i t h o l o g i e s 1) and 3) above

LITHOLOGY

u.

3
0.5-

§

IRMAT IOM

PRE!
|

o

ETERS

ABUI

o

ZONE

AGE

FOSSILCHARACTER

i—

•5

-

R
N
F

.

A
R

G
F

Core
Catcher

Explanatory notes in Chapter 1

j

-40

1

L

j_• "_α_~ '_i

I

' r

I

'

1

I

• '

LITHOLOGIC DESCRIPTION

—

Mi

1
1
_ i - * — , -*— i 1—
1
1.0— j - .j- -i 1

I0s

LITHOLOGIC DESCRIPTION| LITH<3. SAMPLE

Hole

o

Explanatory notes in Chapter 1

DEFORMAT ION

ACMETERS

PRES.

R
N
F

SECTIOABUND.

ZONEFOSSILAGE
MIOCENES i t e 212

moderate yellowish brown(10YR5/4)
3) NANNO SILTb l u i s h white (5B9/1)

Cored Interval: 88.5-98.0 m

Mixed as3

1|2) SILTY CLAY

Core 6FOSSILCHARACTER

Principal lithology:
NANNO SILT
grayish orange (10YR7/4)
Composition:
Nannos92%
Clay
7%
Forams1%
FeldsparTr.
Minor lithologies in order ofdecreasing abundance include:
1) CLAY
grayish brown 5YR3/2

Hole

LITHO.SAM PLE

Site 212
Core is highly disturbed andcontains jumbled mixture ofvarious lithologies.

i

5Y7/2

N9

NANNO OOZEy e l l o w i s h gray above t o
w h i t e below
Composition:
NannosClay
ForamsIron oxide

93-94%
5%
1- 2%
Tr.

Site 212

Core 8Hole

Cored I n t e r v a l : 126.5-136.0 m

Site 212

Hole

Cored Interval: 164.5-174.0 m

FOSSILCHARACTERFOSSILCHARACTER

LITHOLOGIC DESCRIPTION

LITHOLOGIC DESCRIPTION

5Y8/4-EMPTY - x

CLAY, grayish brown (5YR3/2);
probably cavings

Intermixed (disturbed) NANNOOOZE a.nd IRON OXIDE RICH CLAY,
dusky brown (5YR2/2)

Jl
NANNO OOZE
g r a y i s h y e l l o w above t oy e l l o w i s h gray below
Composition:
NannosClay
ForamsIron oxide

5Y6/4

mottles o f
5YR7/288510-

5Y8/4
mottlesof
5Y8/4

f a i n t lamination - 10-20 cm
Section 3 scale of ~1 cm.

NANNO OOZE
dusky y e l l o w (5Y6/4) with zones
of color mottling.
Composition:
Nannos
82-942!
Clay
5-10%
Forams1%
Iron oxide
0- 2%

Core
CatcherHole

Co re 9

Cored I n t e r v a l :ZONE

FOSSILABUND.
PRES.
SECTION

Mixed assemblage

N

A

METERSAGE

1GI I I I | I M l^i I I I

LATE MIOCENEFOSSILCHARACTER

LITHOLOGY

A
R

G
F

Core
Catcher

Explanatory notes i n Chapter 1

General increase i n clay
downward, very s t i f f

36.0-145.5 m

X-ray at 172.80 m Calc
LITHOLOGIC DESCRIPTIONEMPTY~r.AVINGS—

1140.-L•_I_-L•_1_-1

R
N
F

DEFORMATION
LITHO.SAMPLE

Site 212

i÷±÷ü

NANNO OOZE
very pale orange (10YR8/2)
very f a i n t lamination andsubtle m o t t l i n g .
Composition:
NannosClay
ForamsVolcanic glass
Micronodules
Z e o l i t e and p y r i t e

90%
5%
11
\%
1%
Tr.
Core
Catchei
Explanatory notes i n Chapter 1

Site 212

Hole

CorellCored I n t e r v a l : 193.0-202.5 m

Site212LITHOLOGIC DESCRIPTION

CLAY RICH NANNO OOZE
dusky yellow (5Y6/4) withoccasional mottles o f grayish
yellow (5Y8/4)
Composition:
Nannos67-80%
Clay
18-30%
Forams1%
Iron oxide
1%
PyriteTr.
Subtle l i t h o l o g i c (?) m o t t l i n g .

HoleCorel2

Cored I n t e r v a l : 221.5-231.0 m

LITHOLOGIC DESCRIPTION

CLAY RICH NANNO CHALK
dusky yellow (5Y6/4) with spots
and i r r e g u l a r mottles o fgrayish yellow (5Y8/4)
Semilithified.
Composition:
Nannos
82%
Cl ay
15%
Forams2%
Iron oxide
1%
ZeoliteTr.
X-ray a t 228.90 m Calc 98, Quar 1 , Mica 1

Site 212

Hole

Corel3Site 212

Cored I n t e r v a l ; 250.0-259.5 m

LITHOLOGIC DESCRIPTION~°°,l ..„„
lamination

contorted
lamination

contorted
lamination

NANNO RICH MICARB FORAM CHALK
very pale orange (10YR8/2) andmoderate o l i v e brown (5Y4/4)
interlaminated.
General composition:
Nannos2O-3O3S
Micarb
3Q_m
Forams30-40%Clay0- 7%
Others (heavy minerals,
volcanic glass, f e l d spar, rock fragments) <Z%
Very well laminated - alternating l i g h t and dark laminae
generally less than 1 mm thick.
Dark and l i g h t laminae arevariably grouped to produce
alternating l i g h t and dark
sections to the core which range
from 1/2 to 10 cm in thickness.
Other structures include:
1) cross lamination
2) contorted lamination including small 'flame'
structure

Hole

Corel4

Cored I n t e r v a l : 269.0-278.5 m

LITHOLOGIC DESCRIPTION

CLAY RICH NANNO CHALK
grayish orange (10YR7/4)
Composition:
NannosClay
Hicronodules

90%
19%
1%

Site212

Hole

Core 17AGE

LITHOLOGIC DESCRIPTIONZONEFOSSILCHARACTER

Interbedded:a) CLAY RICH NANNO CHALK(as above)b) NANNO FORAM SANDSTONE
bluish white (5B9/1)
well laminated; possibly
graded in lower part.
Contains fragments ofunderlying greenish
clay, and trace of glauconite

sharp
contact

sharp, irregular contact

1 cm

grayish blue green CLAYSTONE (5BG5/2)

5 cm

LITHOLOGY

0.5-

EMPTY

1.0-

S i t e 212

HoleCorelβo

LITHOLOGY

DEFORMATION
LITHO.SAMPLE•=£

Quar 2 8 , Feld 1 9 , Plaq 9 ,Mica 2 5 . Chio 1 . Mont 8

increase z e o l i t e
decrease clay
lighten color

CLAY ZEOLITITE
dark yellowish brown (10YR4/2)
with mottles of moderate brown(5YR4/4).
Zeolite more coarsely crystalline
than above.

LITHOLOGIC DESCRIPTION

EMPTY

CLAY BEARING NANNO CHALK
white (N9) to very pale orange(10YR8/4)
some dark lamination and r i p p l e s

0.51

1

°~

-80
:Z--

--r-———
2r-~-EHrZ i;

—Z

R

Core
Catcher

Explanatory notes in Chapter 1-_->_-_-__:ZEOLITE BEARING IRON OXIDE RICH
CLAYSTONE
dusky brown (5YR2/2) w i t ll
m o t t l e s o f moderate browi(5YR4/4)
Composition:
top bottom
44%
Clay
83%
50%
Ti.
ZeoliteFe-clay aggre10%
5%
gates
:3%
Fe micronodules
Mn micronodules

aol 9,

Cored I n t e r v a l : !97.5-307.0 m

METERS

ZONE

AGE

Q

£

SECTION

Core 16

F DSSI L
CHA RAC ER

Cored I n t e r v a l : 316.5-326.0 m

LITHOLOGIC DESCRIPTIONZEOLITE IRON OXIDE RICH CLAY
dusky brown (5YR2/2)
highly manganiferous
Composition:
Clay73%
Iron oxide micronodules 10?
Clay-iron oxide aggregates5%
Zeolites10%
Mn micronodules
13!
FeldsparTr.
X-ray a t 289.10 n

Hole

ZEOLITE BEARING IRON OXIDERICH CLAY
dusky brown (5YR2/2)

Clays contain abundance ofvery f i n e , high r e l i e f minerals
i n d i c a t i v e of authigenic
mineralization.

Core
CatcherSite 212F

Core
Catchermoderate brown ironoxide rich clay (5YR4/4);r•_--j^.~Z~-

LITHOLOGIC DESCRIPTION

1R
NANNO FORAM CHALK

Cored I n t e r v a l ; 307.B-316.5 m

DEFORMATION
LITHO.SAMPLE

Cored I n t e r v a l ; 288.0-297.5 m

FOSSILCHARACTER

METERS

Hole

FOSSILABUND.
PRES.
SECTION

Site 212

IRON OXIDE RICH ZEOLITE CLAYSTONE
dusky brown (5YR2/2)
Composition:
Clay
45%
Zeolite402
I r o n oxide
14%
Mn micronodules
1%
I r o n oxide occurs as s t a i n i nclay aggregates and as very f i n e
micronodules.
decrease z e o l i t eincrease i r o n oxide
X-ray a t 297.50 m Quar 2 9 , Feld 12, Plag 5, Kao! 18,
Mica 1 7 , Mont 18

X-ray a t 319.70 m Quar 8 , Feld 6 , Plag 3 , Kaol 2,
Mica 6 , Mont 6, Paly 1 6 , C l i n 44,
Phil 8
Explanatory notes in Chapter 1

Site 212

Hole

Core 19

Cored I n t e r v a l ; 326.0-335.5 m

Site 212

Hole

Core 21

Cored Interval: 345.0-354.5 m

HW

FOSSILCHARACTER
LITHOLOGIC DESCRIPTION

LITHOLOGIC DESCRIPTIONNANNO CHALK
white (N9)Composition:
NannosRads
SpiculesDiatoms
Clay

CLAY BEARING NANNO CHALK

white (N9), homogeneous
Composition:
Nannos94%
Clay5%
Spicules1%
Other (glauconite,
micarb, Radiolaria) Tr.
pale green
laminations
and spotsricher in clay

Site 212

Hole
FOSSILCHARACTER

Core 20

Cored Interval.335.5-345.0

LITHOLOGIC DESCRIPTIONNANNO CHALK
white (N9), homogeneous
as core 19
Explanatory notes in Chapter 1

Explanatory notes in Chapter 1

83%
5%
5%
2%
5%

Site 212

Hole
FOSSILCHARACTER

Cored Interval: 354.5-364.0 m

Site 212

Hole
FOSSILCHARACTER

Cored Interval: 364.0-373.5 m

LITHOLOGIC DESCRIPTION

LITHOLOGIC DESCRIPTIONNANNO CHALK
very light gray (N8) withoccasional irregular, graymottles.

NANNO CHALK

σ>very light gray (N8) withoccasional gray clay inclusions
in Section 1
Composition:
Nannos
83%
Rads
5%
Spicules5%
Clay5%
Others (volcanic glass,glauconite, diatom,
micarb
<1%

•~

I I

Composition:
NannosSpicules and Rads
Foram
Other (glauconite,clay, z e o l i t e

95-97%
1- 2%
0- 2%
<U

Green mudstone fragments
present and lamination v i s i b l e
in lower 10-15 cm.

NANNO BEARING ZEOLITE RICH CLAYSTONE
grayish olive green (5GY3/2)
Clay
7<BS
Zeolite24%
Nannos
5%
Other
<U

Core
Catcher
Explanatory notes in Chapter 1

contact disturbed
but sharp
gradational contact
Core
Catcher

Explanatory notes 1n Chapter 1

NANNO CHALK
white (N8) with laminations ofpale yellowish brown (10YR6/2).
Laminations from 1-10 mm thickand range from regular to wavy
to highly contorted (recumbent
folds). Green claystone fragments present in darker
laminations.

Site 212

Hole
FOSSILCHARACTER

Core 24

Cored Interval; 373.5-383.0 m

Site 212

Hole
FOSSILCHARACTER

Core 25

LITHOLOGIC DESCRIPTION

Cored Interval: 383.0-392.5 m

LITHOLOGIC DESCRIPTIONNANNO CHALK
yellowish gray (5Y8/1)

Core
Catcher
NANNO CHALK
very light gray (N8) to pinkish
gray (5YR8/1) with mottles oflight greenish gray (5GY5/1)
scattered throughout
Composition:
Nannos
>95%
Clay
<5%
Other (micarb, glauconite, foraminifera,
Radiolaria, spicules) <2%

Explanatory notes in Chapter 1

Core
Catcher
Explanatory notes in Chapter 1

Site 212

Hole

Core 26

Cored Interval;392.5-402.0 m

S i t e 212

HoleCore 27

Cored I n t e r v a l : 402.0-411.5 m

FOSSILCHARACTER
LITHOLOGIC DESCRIPTION

LITHOLOGIC DESCRIPTIONNANNO CHALK
bluish white (5B9/1)

diagonal f r a c t u r e coated withgreenish CLAY RICH NANNO CHALK

NannosClay
Hicarb
Opaques
Slickensides is apparent

sharp
contact

70%
10%

S2

NANNO CHALK
very light gray (N8) topinkish
gray (5YR8/1).
Composition:
NannosClay
MicarbOthers (glauconite,
foraminifera)<n

NANNO ZEOLITE BEARING CLAYSTONE
moderate brown (5YR4/4)
Composition:
Clay and clay
aggregates
87%
Nannos5%
Zeolite5%
Other (opaques, glass,high relief minerals) 3%"reduced zone"color varies from dark greenish
gray 5G5/1 to medium bluishgray (5B4/1) to greenish black

NO RECOVERY(center) (5GY2/1)
Composition:
Clay and clay
aggregates
ZeoliteVolcanic glass

Other (opaques, highrelief minerals)

88%
7%
2%

3%

uniform moderate brown(5YR4/4)

increasing degree ofrecrystallization(authigenic carbonate)
IRON OXIDE RICH "MINERALIZED"CLAYSTONE

variegated color - moderate
brown (5YR4/4) and dusky yellowish
brown (10YR4/2). Small "flecks"of black scattered through.
Composition:
Clay
68%
Iron oxide-clay
aggregates
5%
Iron spherules
2%
Opaques5%
Zeolite5%

Core
CatcherCore
Catcher

Explanatory notes in Chapter 1

Explanatory notes in Chapter 1

core 28 f o r
description
X-ray a t 403.00 m Quar 1 6 , Feld 10, Plag 3 , Kaol 20,
Mica 20, Mont 31
X-ray a t 403.30 m Calc 3, Quar 18, Feld 14, Plag 6,
Kaol 18, Mica 14, Mont 27
X-ray a t 406.60 m Quar 18, Feld 1 1 , Plag 3, Kaol 22,
Mica 12, Mont 33

3

Core 29

S

o

o

ε

dark reddish brown(10R3/4)

eépale reddish brown(10R5/4)

1

o

N

A

P
V

Bleached (olive) zones containmore ash and zeolite, less ironoxide and high relief minerals
than encasing clays. Reddish
zones are slightly enriched iniron oxides.

ZEOLITE IRON OXIDE BEARING
CLAYSTONE
dark yellowish brown (10YR4/2)
with abundant mottles andirregular "laminae" of1) grayish black (N2)2) light brown (5YR5/6)
Contains also color bands ofchemical alteration as shown
above.
Composition:
Clay
87*
Iron rich clay
aggregates5%
Zeolite4%
Other (opaque, ironmicronodules, highr e l i e f - non-opaqueminerals
4%

EMPTY

Zero section (31 cm) - clay *s
below.

:Z -_-_-.-_-_-_0.5--

LITHOLOGIC DESCRIPTION

V

color band ascore 28

1 0—

100
NANNO SILTSTONE
moderate orange pink

1

pale olive (10Y6/2)

LITHOLOGY<Λ-

Color bands marking 'chemicalalteration 1 . Generally characterized as follows:

EOU

diffuseboundaries

ABUr
PRES

LITHOLOGIC DESCRIPTION

Cored I n t e r v a l : 121.0-430.5 m
WI

FOSSILCHARACTER

DEFO RMAT
LITHC

Hole

CTION

Site 212:TERS

Cored I n t e r v a l : 4 1 1 . 5 - 4 2 1 . 0
FOSSILCHARACTERCore
Catcherdark y e l l o w i s h brown (10YR4/2)
with mottles and i r r e g u l a r streakso f pale reddish brown (10YR5/4J
and grayish black (N2).
Manganese micronodules scatteredthroughout.
Composition:
Clay74%
Zeolite12%
Iron rich clay
aggregates
10%
Other (opaques, glass,authigenic carbonate,high r e l i e f nonopaque)4%

rrj"j•_~_~:(5YR6/4);_

X-ray at 421.30 m Quar 12, Feld 14, Plag 5, Kaol 28,
Mica 23, Chio 11, Mont 6
S i t e 212

HoleCore 30

Cored Interval:430.5-440.0 m

FOSSILCHARACTER
LITHOLOGIC DESCRIPTION

CLAY RICH NANNO CHALK
pale yellowish brown (10YR6/2)
with e l l i p t i c a l "concretions"of grayish orange pink (5YR7/2)
Composition:
Nannos
89%
Clay
10%
Foram
1%
Authigenic c a l c i t e
Tr.

X - r a y a t 4 1 1 . 7 0 m Quar 1 4 , F e l d 1 4 , P l a g 5 , Kao! 2 0 ,Mica 1 9 , C h i o 1 0 , Mont 8 , P a l y 9

i r r e g u l a r color
banding and i n t e r lamination o f paleyellowish brown andgray orange pink

NANNO CHALK
gray orange pink (5YR7/2)
speckled with black manganese
micronodules
Composition:
Nannos85%
Volcanic glass
10%
Opaques (Mn)
4%
Foram
1%

Core
Catcher
Explanatory notes in Chapter 1

Explanatory notes in Chapter 1

Site 212

Hole

Core 31

Site 212

Cored Interval: 440-449.5 m

LITHOLOGIC DESCRIPTION

HoleCore 32

Cored Interval .449.5-459 m

LITHOLOGIC DESCRIPTIONNANNO CHALK
grayish orange pink (5YR7/2)
with occasional elliptical areasof very light gray (N8)Composition:
Nannos92-933!
Clay-5*Forams
1- 2*
Hicarb
1- 2%
NANNO CHALKl i g h t o l i v e gray (5Y6/1)
with mottles of greenish gray

(5GY6/1)
Composition:
NannosClay
MicarbForamvariegatedgray orange pink
and yellowish gray

X-ray at 457.50 m Calc 97, Quar 1 , Mont 2

gradual change from grayish
orange pink to yellowish
gray (5Y8/1)

91%
-5*
3%
1%

O

S i t e 212

HoleCore33

Cored I n t e r v a l : 4 6 9 . 0 - 4 6 5 . 5 m

Site 212

Hole

Core 34

Cored Interval:468.5-478.0 m

FOSSILCHARACTER

LITHOLOGIC DESCRIPTION

LITHOLOGIC DESCRIPTIONNANNO CHALKl i g h t olive gray (5Y6/1) withmottles of l i g h t greenish gray
(5GY8/1) as holes around dark
spots.

Composition as above.

NANNO CHALKl i g h t olive gray (5Y6/1) withoccasional mottles of greenish
gray (5G6/1) which appear asholes around dark spots.

Composition:
NannosClay
MicarbVolcanic glass
Forams95%-Z%
1 - 2%
1%
Tr.

Irregular laminae of paleyellow brown (10YR6/2) in chalkof light olive gray.
Softer than above and richer
in clay and volcanic glass.
Composition:
Nannos87%
Clay5«
Volcanic glass
3%
Forams2%
Micarb2%
Opaques1%
Explanatory notes in Chapter 1

100

Explanatory notes in Chapter 1

Site 212

Hole

Core35Site 212

Cored Interval:478.0-487.5 m

Hole

Cored Interval: 487.5-497.0

LITHOLOGIC DESCRIPTION

LITHOLOGIC DESCRIPTIONNANNO CHALK
X-ray a t 481.80 π Calc 92, Quar 1 , Feld 1 , Plag 1 ,Mica 2 , Mont 2
X-ray a t 483.30 m Calc 94, Quar 1 , Feld 1 , Mica 2,Mont 2
X-ray a t 484.10 m Quar 13, Feld 1 1 , Plag 6, Kaol 3,
Mica 13, Chio 1 , Mont 4 3 , Paly 9
X-ray a t 484.40 m Quar 17, Feld 16, Plag 6, Kaol 5,
Mica 8, Chio 1 , Mont 22, Paly 2 1 ,Hema 3

Zeolites very poorly c r y s t a l l i z e d .
X-ray a t 488.60 m Quar 24, Feld 16, Plag 8, Kaol 3,
Mica 13, Chio 2, Mont 9, Paly 26

color banded (1 cm bands)
greenish gray with lightolive gray (5Y6/1)

green mudstone
fragments in lower
70 cm of chalk

FORAM NANNO CHALK
NannosForamsMicarbClay
Volcanic glassR|
LITHOLOGY
DEFC

;
z z z
0 . 5 — ü-Z-I : z z z
z zz
I H-£HJ I Z Z Z
1z z z: z z z1.0—z z z
z z z zIz z z :z z z zCorez z z ;
Z z zzCatcherz z z

CLAYSTONE, grayish green (5G5/2)

IRON OXIDE RICH CLAYSTONE
dark reddish brown (10YR3/4)
Composition:
Clay
6
Iron rich clay aggregates3
ZeoliteOther (Fe micronodules,
high relief nonopaque)| LITHILITHOLOGIC DESCRIPTION

1

ABU

PRE:

|

Cored Interv a l : 497.0-506.5 m'1 '1 '
'1 '1 '1
I I I

greenish graywith whitemottlesincreasing foram
content; coarsening
texture

|

AGE

Q

2
greenish gray
5GY6/1

Core 37

FOSSILCHARACTER

IETERSHole

ET 101

S i t e 212

ZONE

NANNO CHALKl i g h t o l i v e gray (5Y6/1) with
abundant mottles o f greenish gray
(5GY5/1) and l i g h t greenish gray(588/1)
Composition:Naπnos812
Micarb10*
Forams8%
Volcanic glassλ%

ZEOLITE CLAYSTONE
moderate reddish brown (10R4/6)
Composition:
Clay
503!
Zeolite40$
Fe r i c h clay aggregates 2%
Volcanic glass
Z%
Other (very fine highrelief minerals,
opaques, feldspar
6%

uniform
5YR4/4-92-98

5YR4/4 banded
a t 1-8 cm scale
w i t h 10YR2/2

CLAY RICH ZEOLITITE
to dusky yellowish brown
General composition:
Zeolite60-70%
Clay
20-30%
Opaques
1 - 3%Fe micronodules
1-4%
Others (very f i n e highr e l i e f non-opaque,s i l t sized feldspar <2%
Zeolites - well c r y s t a l l i z e dlaths averaging 12-15 m i n length.
Light colored layers contain lessopaques and Fe micronodules thandark layers.
X-ray a t 497.30 m Quar 23, Feld 14, Plag 2, M1ca 8,Mont 5, Paly 48

Explanatory notes in Chapter 1
Explanatory notes in Chapter 1

alternating
5YR5/6 and5YR3/2 occasional
greenish mottle

1

1

ABUND. |PRES.

j

LITHOLOGIC DESCRIPTION

Cored Interv a l : 516-521 m

Core 39

FOSSILCHARACTER

1

LITHOLOGY-

CLAY ZEOLITITE
light brown to grayish brown

1 Flow

1CU

1 LITHO.SAM

Hole

1 DEFORMAT ION

Site 212

SECTIOI

Cored Interval: 506.5-516.0 m|

Core 38

1 FOSSIL

Hole
FOSSILCHARACTER

ZONE

Site 212[ AGE

LITHOLOGIC DESCRIPTION?

a
0 . 5 - :, _' = s-v' *t/\ b
I, 1 , 1 , 1 ','«-*«', cd
1.0—

Thin QPrtinn
1' " bπ i JCCLIUπ
a tcm- /v* ,"****/»*

grayish green (10GY5/2)
to yellow green (5GY7/4)

decreasezeoliteincreaseiron oxided2 Flow
IRON OXIDE RICH ZEOLITE CLAYSTONE
grayish brown
Composition:
Clay
55%
Iron oxide clay aggre20%
gates
Zeolites
4%
Fe micronodules
Opaques
Authigenic carbonate

Core
Catcher

2—~—__

3 FlowIe- * X*r">*^^;becThin section
149 cm.
(Basaltic glass)I—_ V **"«•" * £ l i a• \ • » r • " à > ^ á - ' ' t

e

3

e
c
!

_
—
_
-

5

_
—
_
-

I
6

2
I
—
""

Core
Catcher
Explanatory notes i n Chapter 1(Basaltic .lass)(Limestone)

X-ray a t 507.20 m Quar 13, Mica 5 , Mont 1 1 , Paly 52,
C l i n 19
X-ray a t 508.20 m Quar 19, Feid 34, Mica 12, Paly 36

4(Basaltic glass)

b

—
_
-

b a s a l t i c rock fragments
Explanatory notes i n Chapter 1

Thin section(a) very l i g h t gray (N8) LIMESTONE
Calcite95%
Plagioclase<5%( b ) CHLORITE BEARING BASALTIC GLASS
πrftdnich hlark ^ P V 9 / l l
Palagonite
40%
Glass
50%
Chlorite
10%(c) MEDIUM GRAINED SPILITIZEDBASALT

'

Mill

ON
NJ

>

l.^

;

'ç

J

ft

Λ

c

(5GY5/1). Hypocrystalline medium grained and weatheredbasalt. Microphenocrysts ofp a r t i a l l y albitized Plagioclase
are set into an intersertal
matrix of Plagioclase (probably
albitized). Pyroxene granules,
dark brown mesosrasis (ironoxide granules and brown glass),
chlorite and cryptocrystalline
material occur between theinterstices of the Plagioclase
laths. The Plagioclase microphenocrysts and the Plagioclase
from the matrix often show
inclusion of c h l o r i t e , calcite

^p
p u

^

afe‰Hx 47%
M i c r o p h e n o

.

cryst
10%
Chlorite
15%
Mesostasis
10%
Calcite7%
Pyroxene
6%
Epidote<1%
Palagonite
1%
Iron oxide
3%(d) VOLCANIC BRECCIA fragments ofbasaltic glass in c a l c i t i ccement one foram was foundwithin the carbonate cement.
Calcite75%
Spil itized basalt
fragment
15%
Basaltic glass
10%(e) FINE GRAINED SPILITIZED BASALT
medium olive gray (5Y5/1). This
zone often grades into a glassy
margin and consists of porphyr i t i c weathered rock. Phenocrysts
and microphenocrysts of olivine
outlined crystals and partiallyalbitized Plagioclase are set
in a v a r i o l i t i c and p a r t i a l l y
crystalline matrix.
Plag. microlite
40%
Plag. micropheno.
5%
Plag. phenocryst2%
Mesostasis
39%
Olivine outlined
crystals
6%
Chlorite
35?
Calcite2%
Cristobalite
2%
Volcanic glass
1%

SITE 212

212-1-1

212-1-2

212-1-3

212-1-4

212-1-5

212-1-6
63

SITE 212

0 cm

— 25

j

!

Λ

50

— 75

•

100
(

—125

mβmá

150

212-2-1
64

212-2-2

212-2-3

212-2-4

212-2-5

212-3-1

SITE 212

r

0 cm

— 25

— 50

— 75

—100

—125

L

150

212-4-1

212-5-1

212-7-1

212-8-1

212-8-2

212-8-3
65

SITE 212

•0 cm

25

50

75

100

125

150

212-9-1
66

212-10-1

212-10-2

212-10-3

212-10-4

212-10-5

SITE 212

0 cm

25

50

75

100

125

150
212-10-6

212-11-1

212-11-2

212-11-3

212-11-4

212-12-1

67

SITE 212
0 Cm

25

50

75

100

125

150

212-12-2
68

212-12-3

212-12-4

212-12-5

212-13-2

212-13-3

SITE 212

212-13-4

212-14-1

212-14-2

212-14-3

212-14-4

212-14-5
69

SITE 212

212-14-6
70

212-15-1

212-15-2

212-15-3

212-16-1

212-16-2

SITE 212

0 cm

25

50

75

100

125

150

212-17-1

212-18-1

212-18-2

212-18-3

212-19-1

212-19-2
71

SITE 212

0 cm

25

— 50

— 75

—100

125

150

212-20-1
72

212-21-1

212-21-2

212-21-3

213-21-4

212-22-1

SITE 212

0 cm

25

50

75

100

— 125

150

212-22-2

212-22-3

212-22-4

212-23-1

212-23-2

212-23-3
73

SITE 212

212-23-4
74

212-23-5

212-24-1

212-25-1

212-25-2

212-25-3

SITE 212

0 cm

25

50

75

100

125

150

212-25-4

212-25-5

212-25-6

212-26-1

212-26-2

212-26-3
75

SITE 212

0 cm

— 25

— 50

— 75

—100

125

150

212-26-4
76

212-26-5

212-26-6

212-27-1

212-27-4

212-27-5

SITE 212

•0 cm

25

50

75

100

125

150

212-27-6

212-28-1

212-28-2

212-28-3

212-28-6

212-29-1
77

SITE 212

0 cm

25

-

50

— 75

—100

—125

150

212-30-1
78

212-30-2

212-30-3

212-31-1

212-31-2

212-31-3

π

•0 cm

SITE 212

|

I

9

1

— 25

— 50

— 75

—100

11

—125
i

k.

i

M

150

212-31-4

212-31-5

212-32-1

212-32-2

212-32-3

212-32-4
79

SITE 212150

212-32-5
80

212-32-6

212-33-1

212-33-2

212-33-3

212-33-4

SITE 212

Ocm

25

50

75

100

125

150

212-33-5

212-33-6

212-34-1

212-34-2

212-34-3

212-35-1
81

SITE 212

0 cm

— 25

•

•

— 50

75

;

•

•

.

*

100

—125

1]
150

212-35-2
82

212-35-3

212-35-4

213-35-5

212-36-1

212-37-1

SITE 212

150

.38-1
212

212-38-2

2 12 -38-3

212-39-1

212-39-2

212-39-3
83