2. SITE 211
The Shipboard Scientific Party1

ABSTRACTAt Site 211, early Campanian and Maastrichtian nannofossil
ooze, clay, and ash overlay a weathered and alteredamphibole-bearing basalt basement at a sediment depth of 435
meters. The next younger unit is a ferruginous brown clay,
intruded near its base by a 10-meter-thick diabase sill. A
200-meter-thick unit of interbedded sands and siliceous oozes
overlies the brown clay. The sands are turbidites of Pliocene age
and form part of the Nicobar Fan. The uppermost 100 meters of
the hole yielded pelagic siliceous oozes and ash beds of late
Pliocene and Quaternary age. The ash beds probably originatedfrom island arc volcanism to the north.
SITE DATA

Date Occupied: 21 Jan 72 (0830)
Date Departed: 24 Jan 72 (1030)
Time on Site: 74 hours
Position:lat 09°46.53'S
longl02°41.95'E
Water Depth (to rig floor):
5528 meters (echo sounding)
5535 meters (drill pipe)
Penetration: 447 meters
Number of Holes: 1
Number of Cores: 15
Total Length of Cored Section: 142.5 meters
Total Core Recovered: 67.21 meters
Acoustic Basement:
Depth: 5970 meters
Nature: Basalt
Age of Oldest Sediment: Early CampanianBasement: Basalt
BACKGROUND AND OBJECTIVES

The initial drilling plan for Leg 22 in the Indian Ocean
called for four sites in the Wharton Basin. The first twosites were close to each other at 9°34.9'S, 102°01.4'E and
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.

7°20.0'S, 100°14.8'E and were picked to determine
basement age on the gentle swell seaward of the Java
Trench and to examine the differences between two
apparently different seismic reflection records. After thepresite surveys by R/V Robert Conrad, it was discoveredthat these differences in the records were very local andthat both sites showed the same general sediment character.
We decided to drill the first site and to consider the second
as an alternate should we have problems. Site 211 waslocated on a flat topographic region on a gentle rise just to
the south of the Java Trench and has a depth of close to5500 meters (Figure 1). The area of the site is bounded to
the north by the trench, to the west by the Nicobar
Fan—an extension of the Bengal Fan east of the Ninetyeast
Ridge—to the south by Cocos Keeling Plateau, and to theeast by Christmas Island,
The seismic reflection records in the area arecharacterized by a transparent layer about 0.1 to 0.3 sec
thick on top of a more opaque and diffuse layer of some
0.2 sec. Throughout the area a topographically roughbasement can be observed at 0.4 sec depth. However, in
isolated regions the basement crops out at the surface. The
seismic reflection record from the Challenger at the site isfairly typical of the region, and the prominent features ofthis record can easily be recognized on the form contours
from the Conrad 14 presite survey (Figure 2). The seismicreflection records (this chapter and Chapter 10) show that
Site 211 was selected in a small basin with three prominentsubsurface reflectors. The bottom reflector was assumed to
be basement at a depth of 0.45 sec.
The objectives of this site were to date the basement age
and to identify the prominent reflectors on the seismic
record.
OPERATIONS

Site 211 was approached along a course of 270° in orderto verify a seismic line from the presite survey of the R/VRobert Conrad. The site was selected in a sediment basin
approximately 12 nautical miles in length, containing
about 0.4 to 0.5 sec of sediment overlying basement. The
site chosen is about 15 nautical miles east of the13

SITE 211
7C

Tl

8°

33b

10°-

102°

103°

104'

105 c

Figure 1. Bathymetry and magnetic anomalies in vicinity of Site 211.
recommended site, the choice being governed by thepresence of less intense seismic reflectors in the new site
compared with the original selection. A spar buoy was
dropped over the proposed drilling location, after which theseismic gear was secured and the vessel reversed course to
the buoy.
Coring was planned on the basis of one barrel every 30
or 40 meters of drilling, with continuous coring in thebasalt section. A 4-cone chizzel-point bit was used, and a
total of 15 cores was ultimately recovered (Table 1).
The unconsolidated siliceous pelagic ooze of theuppermost 100 meters was sampled by employing

14

controlled pump pressure to avoid washing. The underlying
turbidite sand sequence was successfully cored, although it
provided some anxious moments due to sand flowage.
Fortunately, deeper sands contained sufficient clay tostabilize the hole. Difficult drilling conditions wereobtained in stiff brown clay section below the turbidite due
to bit clogging. A 10-meter-thick sill was cored without
difficulty near the bottom of the hole, followed by stiff
calcareous clay and finally basaltic basement. The stiff
calcareous clay again caused problems by clogging the bit.
However, the basalt basement was cored without difficulty
to a thickness of 12 meters, with 60% recovery.

SITE 211

Figure 2. Presite survey and form lines for Site 211.
LITHOLOGIC SUMMARY
Introduction

4

At Site 211 Quaternary to lower Campanian sediments
were penetrated to a depth of 428 meters, below which
weathered basalt was recovered. Coring was attempted for
143 meters from which 54 meters of sediment and 13
meters of igneous material were obtained (Figure 3). The
following lithologic units can be recognized.

Unit

Depth
Below Sea
Floor (m)

1 0 to 95
2 95 to -200

3 -200 to
-335

5
6

7

Lithology

Age

Cores

Clay-rich siliceous
ooze with volcanicash beds
Rad-rich clay or
clay-rich rad ooze
with abundantsilt/sand at top
decreasing
downward
Clayey silt/silty
sand decreasing in

Quaternary to
upper Pliocene

1-3

Pliocene

4-6

Pliocene to
Miocene (?)

7-9

grain size downwards to silty clay
9
Brown clay passing-335 todown into amorphous-401.5iron oxide andpyrite-rich ash facies7
401.5 to 411.5 Diabase sill
Basal Maas411.5 to 428.5 Variegated gray,cream, and red nanno trichtian toBasalooze and clay
Campanian7428.5 to 447 Weathered amphibole-bearing basalt
and amphibolite

10-11

12

12-14

14-15

Description

Unit 1—Clay-rich Siliceous Ooze with Volcanic Ash Beds
(Cores 1-3)This unit is mostly siliceous ooze with a small admixture
and a few thin (>15 mm) interbeds of volcanic ash. The
major components of the siliceous ooze are diatoms, butRadiolaria, sponge spicules, and, to a lesser extent,

15

SITE 211
TABLE 1
Coring Summary, Site 211

Date
Depth from
Depth Below Length
Recovered Recovery
Core (Jan) Time Drill Floor (m) Sea Floor (m) Cored (m)
(m)
(%)
1

22

2

22

3

22

4

22

5

22

6

22

7

22

8

22

9

22

10

23

11

23

12

23

13

23

14

23

15

23

0025 5535.0-5544.0
0230 5544.0-5553.00450 5592.0-5601.5
0720 5630.0-5639.5
0935 5668.0-5677.5
1220 5715.5-5725.0
1520 5763.0-5772.5
1800 5791.5-5801.0
2110 5829.5-5839.00015 5877.0-5886.00315 5924.5-5933.01120 5944 0-5953.5
1410 5953.5-5963.0
1635 5963.0-5972.5
2220 5972 5-5982.0

0-9.0
9.0-18.0
57.0-66.0
95.0-104.5
133.0-142.5
180.5-190.5
228.0-237.5
256.5-266.0
294.5-304.0
342.0-351.0
389.5-398.0
409.0-418.5
418.5-428.0
428.0-437.5
437.5-447.0

Total

9.5

9.0

100

9.5

9.0

100

9.5

7.5

83

9.5

3.8

43

9.5

7.9

83

9.5

9.5

100

9.5

1.5

20

9.5

1.1

14

9.5

3.7

40

9.5

0.6

6

9.5

(co

0

9.5

3.1

35

9.5

1.3

15

9.5

3.4

37

9.5

5.7

62

142.5

67.1

47.2

Note: Echo sounding depth (to drill floor) = 5528 meters;
drill pipe length to bottom = 5535 meters.

silicoflagellates are also common. Clay minerals of
terrigenous and volcanic origin are abundant in the ooze,
and in places the sediment becomes a radiolarian-rich clay.
Glass shards, feldspar, and pumice fragments make up lessthan 10% of the siliceous oozes. The volcanic ash ismostly (50%•90%) made up of fresh clear rhyolitic glass
shards of silt and fine sand size, the remainder of thecomponents being clay minerals, quartz, feldspar, andheavy minerals.
Unit 2—Radiolarian-rich Clay or Clay-richRadiolarian Ooze with Silt and Sand (Cores 4-6)
In this unit clay with siliceous fossils, similar to Unit 1
except that Radiolaria are more abundant than diatoms, isinterbedded with terrigenous silt and sand. In the lower
part of the unit (Core 5, 6) the clay is predominantly of
volcanic origin (see X-ray data).
The terrigenous material is highly feldspathic (up to60%), the feldspathic component seen in smear slides
consisting almost completely of orthoclase with minor
microcline and sodic Plagioclase (this is in direct contrast to
the X-ray data). Biotite and muscovite are present inamounts of 15% to 30%, while smaller amounts of clay andminor quartz and heavy minerals make up the remainder.
Unit 3-Clayey Silt/Silty Sand to Silty Clay (Cores 7-9)
This is similar to the terrigenous component in Unit 2
and makes up all of this unit, the major variation being thepresence of finer-grained, silty clay beds interbedded withthe silty sands lower down. Heavy minerals have beententatively identified as belonging to the hornblendeepidote suite. Mica appears to be less common here than in
the terrigenous component on Unit 2.

16

In Core 7 a few rounded fragments of indurated
calcareous siltstone were seen and are presumably reworked
from elsewhere.
Unit 4 —Brown Clay, Amorphous Iron Oxide,and Pyrite-rich Ash Facies (Cores 10-11)
Two cores in this unit show a transition fromiron-oxide-rich brown clay to an amorphous iron-oxidefacies with three distinct sediment types: (1) moderate
brown homogeneous amorphous iron-oxide (with aconsistency of firm clay) comprising 70% iron-oxideminerals, 20% clay minerals, and 10% remanats of glass
shards, feldspar, and heavy minerals; (2) moderately
indurated dark gray, pyrite-rich ash which is dominantly(80%) devitrified basaltic glass shards almost totallyreplaced by iron-oxide. Pyrite and less common minutegrains of iron-oxide minerals make up the rest of thesediment; (3) moderately indurated red ash-rich iron oxide.
This sediment is about 90% iron aggregates, many of which
are hematitic with 10% remnant altered glass shards similarto (2) above. Traces of feldspar and cristobalite (?)
aggregates were seen.
Unit 5-Diabase Sill (Core 12)
Unit 5 is a 10-meter-thick igneous intrusive phaneritic
rock with a diabasic texture. While most of the anhedraland subhedral plates of clinopyroxenes are partiallyenclosed by Plagioclase laths, only few larger pyroxenes
show poikilitic inclusions of Plagioclases. The Plagioclase (2to 3 mm in length) comprise about 40% of the bulk rock.
Clinopyroxene is the next most abundant (< 25%) mineral.
Phyllosilicates (21%) comprising serpentine and mixed layerof vermiculite-chlorite occur. The minor constituents

SITE 211
SITE 211

hypocrystalline fine-grain rock with an intersertal texture.
The interstices of the Plagioclase laths are filled withpalagonite, calcite, iron oxide, and granules of clinopyroxene. This lower part of the sill probably represents achilled margin.

09°46.5'S 102°41.9'E
5535 m
Rad Diatom
Ooze & Ash

QUAT.

PLIO.

Diatom Ooz

S i l t y Sand
Clay

-100

Rad Clay,Silt

Rad Ooze-200

Clayey Sand

Clayey S i l t

i l t y Sand

10

? 11

12

WEST.
'13AMP.
-14 =
15:

300

rown Claye-Fe

eO, Pyrite
iabase400
411.5

anno Clay
428.6
asal t\mphibolite
asalt

T.D. 447 m; 15 c o r e s ;67 m r e c .

Figure 3. Lithologic units at Site 211.
consist of iron ore (5%) often surrounded by flakes of
biotite (7%) and needles of amphibole (<3%). Calcite,
zeolite, and pyrite occur as accessory minerals throughout
the unit. Calcite and aggregates of süiceous material occur
as inclusions in the most sodic Plagioclase laths.
The upper contact was not cored. The lower contact of
the sill was recovered and comprises about 20 cm ofUnit 6—Variegated Nannofossil Ooze, Nannofossil
Clay, and Iron-rich Ash (Cores 12-14)
This unit comprises rapid alternations of red, cream, andgray nannofossil-rich clay, nannofossil clay, and nannofossil
ooze. In addition to nannofossils and clay minerals,
feldspar, zeolite (?), dolomite, and heavy minerals also
occur.
Immediately beneath the "andesitic" diabase sill thesediment is a dusky red, but this red color which is due toiron minerals, fades out quickly so that 20 cm below thecontact the color is only light brown to gray orange. A few,
rare, iron-rich ash beds also occur and consist of strongly
altered volcanic glass, mostly replaced by iron-oxideminerals with incipient Plagioclase and palagonite, andcommon heavy minerals (goethite or limonite andhematite) with feldspar, nannofossils, and mica.
Unit 7—Weathered Amphibole-bearing Basalt(Cores 14, 15)This unit consists of phaneritic (coarse-grained) andaphanitic (fine-grained) weathered basalt. Often thephaneritic basalt grades towards aphanitic abundantly
altered zones. Such a sequence was recognized 12 times
within the 8 meters of cored basalt. These alternatesequences of textural changes accompanied by grain-sizechanges could be attributed either to the presence of several
laval pillows or to a series of separate flows.
The phaneritic basalt zone has a hyalopilitic texture
where the interstices of the plagioclases are filled with adark mesostasis. This latter zone also contains abundant
amygdales. The aphanitic basalt zone has a variolitic texture
in which radiating clusters of feldspar laths are set in amatrix of weathered mesostasis. Little fresh glass was foundin the core.
Amphibolite (Core 14, Section 2 andCore 15, Sections 1, 2)
These rocks are intruded within the amphibole-bearing
basalt. The amphibolites form several flows (about four)with sharply defined and altered margins. The inner portionof the amphibolites are more crystalline and coarser
grained. These amphibolites are made up of about 80%
amphiboles, olivine and mica, with 20% calcite andgroundmass.
GEOCHEMISTRY PROGRAM

Samples were collected from 11 of the 12 cores whichcontained more than a kilogram of sediment. The samplingtechnique and handling procedure is described in Chapter 1.
The recovery from Core 7 (1 section) was judged to beunsuitable for sampling because of the large quantity offreely moving water retained in the core liner. Samples
from Cores 1 through 6 and Core 9 were obtained andprocessed immediately upon recovery. Samples from Cores8, 12, 13, and 14 were taken after the cores had been in the17SHE 211

laboratory for a full day or more. A summary of the results
is given in Table 2.
In the case of Core 8, the sediment sample was takenfrom the split core section by the method described in theInterstitial Water Program Instruction Manual, Chapter 1,
Section 5. Small "biscuits" of unsplit, indurated sedimentwere taken from Cores 12, 13, and 14. These sediments had
been standing in trays fashioned from split plastic liner
since being opened for initial inspection immediately uponrecovery. Drying was retarded by using the other half of the
split liner as a cover. The sediments were moist to the touchat the time of sampling. Handling was kept to a minimum,and entire portions were squeezed to the maximum limit of
the hydraulic press in order to obtain sufficient amounts of
fluid for the minimum pore water program.
BIOSTRATIGRAPHY SUMMARY
GeneralThe 15 cores obtained from Site 211 include sediment
ranging in age from Quaternary to Late Cretaceous(Campanian).
Cores 1, 2, and 3 yielded well-preserved radiolarians.
Cores 1 and 2 are Quaternary in age, and Core 3 is late
Pliocene. The Pliocene/Quaternary boundary presumably
occurs in the uncored intervals between Core 2(18 meters)and Core 3 (57 meters).
Cores 4, 5, and 6 contain moderately well preserved
radiolarian species which are indicative of a middle to late
Miocene age. This assemblage is probably reworked,
however, because the underlying material in Cores 7
through 9 appears to be younger.
Cores 7, 8, and 9 are no older than Pliocene in age, basedon scattered specimens of Sphaeroidinella dehiscens within
the sandy layers.
Cores 10 and 11 are barren of microfossils.
Core 12 contains nannofossils diagnostic of the lateCampanian to early Maastrichtian.
Cores 13 and 14 are early to middle Campanian in age,also based on nannofossils.
Average rates of sediment accumulation in Cores 1
through 3 are 10 to 25 m/m.y. In Cores 4 through 9 theaverage accumulation rate appears quite high, in the rangeof 50 to 100 m/m.y. In Cores 12 through 14 the averageaccumulation rate is 3 m/m.y.
Foraminifera

The important Cenozoic assemblages occur in the sandy
beds in Cores 7 through 9 and undoubtedly have beenreworked from the shelf and slope. Specimens occur
sporadically, but there is an overall consistency. Shallowwater tropical benthonics {Pseudorotalia, Elphidium) tend
to be more battered than those from deeper water(Bolivina, Uvigerina, Bulimina, Hyalinea, Oridorsalis, etc.).
The planktonic pseudo-assemblages in Cores 7 through 9
indicate a maximum age of Miocene or younger:
Globigerinoides trilobus sicanus (N.8-N.9, early Miocene);
Globorotalia tumida s.s. (N.I8, late Miocene); Sphaeroidinella dehiscens (N.19, early Pliocene). It is stressed that theconsequent maximum age of early Pliocene for these sands,
presumably turbidites, is based on single specimens of

18

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

Water
(%)

Porosity(%)

Density(gm/cc)1-1, 90
1-2, 125
1-3,07.7
1-5, 90
1-6,4

77
67
71
65
67

96
88
92
90
89

1.25
1.31
1.28
1.39
1.32

7.4

69

91

1.32

7.4

64
65

86
91

1.34
1.41

7.1

26
63
42

49
85
68

1.93
1.35
1.63

7.2

63
23
45

87
48
73

1.38
2.07
1.63

24
25
62

50
50
87

2.04
1.95
1.41

8-1, 89 7.6
8-1,120

16

32

2.06

9-2, 133
9-3,0
7.8
9-3,140

24
15
15

46
34
33

1.94
2.24
2.19

11, CC

30

-

-

-

-

2-3,0
3-1, 853-4,0
4-2,204-2,764-3,0
5-2, 30
5-4,71
5-5,0
6-5,0
6-5,7
6-6, 50

12, CC

7.1

7.3

36

13-1,55 7.1

32

-

-

14-1,12 7.3

26

-

-

Sphaeroidinella dehiscens in each of Cores 7,8, and 9, butthat no other explanation (drilling or laboratory contamination) seems adequate. The source of this fossil material was
tropical, where the range of Pseudorotalia is not wellknown, but its occurrence suggests an upper Miocene to
Pliocene rather than an older age.
Foraminiferal assemblages in Cores 12 through 14 arecharacterized by (1) no planktonics, (2) both agglutinatedand secreted-calcareous benthonics, (3) small size andpreponderance of earlier ontogenetic stages in several
instances, and (4) evidence of test thinning by carbonate
solution. The presence of Angulogavelinella praecaucasica,
Alabamina dorsoplana, and Reussella sp. indicates acorrelation with the Korojon Calcarenite (Carnarvon Basin,West Australia) and a late Senonian to Maastrichtian age.
Variations in the presence and amount of Inoceramus
prisms are noteworthy.
With respect to the Korojon Calcarenite—the only usefulcomparison at present—these assemblages lack large
Gaudryina, Dorothia, Marssonella, and large and strongly
calcified anomalinids/gavelinellids and contain Glomospirain probably a more agglutinated overall character. All
species are known from shelf sediments. Environmentally,
it would seem that one is perhaps forced to choose between
two extremes. The situation might have been inshore to thepoint where planktonic foraminifera were excluded, but
not calcification by benthonics and Inoceramus (nor

SITE 211

calcareous nannoplankton). There are precedents for this.
However, no palynomorphs were found in a sample
submitted to W. K. Harris, whereas response to H2O2
indicates the presence of organic matter. Alternatively,
depth was sufficiently great to affect significantly thenannofossils and remove entirely the planktonic foraminifera by solution, but not several calcified benthonics(whether in situ or by downslope movement).
Nannofossils
Calcareous nannofossils were recovered only within theinterval between the diabase sill and the volcanic basement.
This interval is approximately 18 meters thick and consistsof irregularly laminated, highly calcareous sediments of late
Cretaceous age. The nannofossil assemblages are ratherpoor, owing, it appears, to selective solution of the majorityof species. Relatively precise age assignments can be madebecause the index species, happily, seem to have been themost resistant to corrosion. The sediment recovered in Core12, immediately beneath the diabase sill, has as its mostabundant constituent the index species Tetralithus nitidus
trifidus, indicating a late Campanian to early Maastrichtianage. Core 13 and the top of Core 14 contain essentially thesame assemblage, except that Tetralithus nitidus trifidus islacking. The presence of Bronsoina parca, however,indicates that the sediment is not older than the early to
middle Campanian Eiffellithus augustus Zone. Apparently
the transition between the two zones was lost between
Cores 12 and 13, or alternatively, a hiatus separates thesediments of the two cores.
It is noteworthy that among the variegated laminae inCores 12, 13, and 14, the light-colored (tan to pale yellow)
laminae contain the largest number of recognizable
nannofossils, while red and brown laminae generally
contain few recognizable specimens. But even in the palelayers, complete nannofossils constitute only a small
portion of the calcareous fraction, and by far the greatest
percentage of the sediment consists of corroded, unrecognizable fragments of coccoliths.
This may be explained by assuming that the above
sediments were deposited near the carbonate compensation
depth and that most of the calcareous nannofossils werepartially or completely dissolved. Only the forms mostresistant to solution remained intact. This idea is supported
further by the low accumulation rate for these sediments. If
we assume that the 18 meters of sediment between
basement and the diabase sill represent most of Campaniantime (about 6 million years), a sedimentation rate of 3
m/m.y. is obtained. This rate is about one tenth of theaccumulation rate for pelagic calcareous ooze, and somemechanism is required for removing a large part of thesediment. Selective solution of carbonate seems one
possible explanation.
Radiolaria
Within Cores 1 and 2 the radiolarian assemblages consistof well-preserved specimens of Lithopera bacca, Ommatartus tetrathalamus, Theocorythium trachelium, Eucyrtidium hexagonatum, Pterocanium praetexum, and Lamprocyclas maritalis maritalis. The absence of Pterocanium
prismatium indicates a Quaternary age for these two cores.

In Core 3 the presence of Pterocanium prismatium, in
addition to the species of Cores 1 and 2, and the absence ofStichocorys peregrina indicate a late Pliocene age.
Cores 4 through 6 contain radiolarian assemblages which
are poorly to moderately well preserved. The species mostcommon in these cores are diagnostic of the middle toupper Miocene C. petterssoni and 0. antepenultimus zones.
However, the presence of scattered specimens of Sphaeroidinella sp. in the underlying Cores 7 through 9 (seediscussion of foraminifera) suggests that Cores 4 through 6
may be Pliocene in age and that the Miocene forms are
reworked. Hence, a Pliocene age is assigned to Cores 4
through 6.
CORRELATION OF REFLECTION PROFILEAND STRATIGRAPHIC COLUMN
Figure 4 illustrates the correlation between thegeneralized stratigraphic column of Site 211 and the airgun
seismic reflection profile of the area. It is evident that theuppermost unit, a 95-meter-thick Quaternary-Pliocene
siliceous ooze with ash beds, correlates well with the upper
acoustically transparent zone on the seismic record. Below
this the first major seismic reflector (1), which is rather
broad and ill defined, correlates with the uppermost of aseries of turbidite sands and silts. The underlying broad
seismic reflector (2) lies within the turbidite sequence at
225 meters, with the intervening acoustically transparent
zone possibly representing a more pelagic interval within
the turbidites, with fewer sand beds. The acousticallytransparent zone below the second reflector correspondswith a sequence of sands and brown, nonfossiliferous clays
which are intruded at their base by a 10-meter-thickbasaltic andesite sill. Seismic basement on the airgun
record, broad and ill-defined in this area, probably
represents this sill. The basal basalt is separated from the sillby approximately 18 meters of thinly bedded red-brown,
clayey, nannofossil-bearing sediment which is not readily
identifiable on the seismic record.
Depths of reflectors and interval velocities are as
follows:
Reflector

2-Way Time
(sec)

0
1
2
3

0.11
0.24
0.41

0

Depth
(m)
0
95
225

Interval Velocity(km/sec)

2.0

401.5

SUMMARY AND CONCLUSIONSThe site for Hole 211 was selected approximately 3300
km west-northwest of Christmas Island and 1800 km southof the Java Trench. The hole, in a water depth of 5525
meters, was drilled in a basin of draped strata overlying
ponded sediments. The surrounding topography is smooth
except for a small seamount situated about 18 km to thesouth of the site.
The deepest lithological unit cored at Site 211,
presumably oceanic basement, is a weathered, amphibolebearing basalt which contains an unusual intercalated
amphibolite in the form of a sill with chilled margins. This

19

SITE 211

metersSITE 211

0 -c

Radiolarian-diatom
ooze with ash beds

100

Turbidite clayey
sands, interbeddedwith siliceous
oozes
200-

300-

Brown clays

400
Diabase sill

401.5CTayëy~~na nno~~oözeT
red -br own-^g ray__Basaltic basement
Figure 4. Correlation of reflection profiles and stratigraphic column at Site 211.
20

Nautical MilesSITE 211

amphibolite is believed to be igneous and not metamorphic.
The weathered amphibole-bearing basalts are considered to
be extrusives, possibly pillow lavas which have been alteredby the subsequent amphibolite intrusives as well as bysubmarine weathering processes.
The oldest sediment unit encountered at Site 211 is avariegated gray, cream and red-brown, nannofossil-bearing
clay of early Campanian to Maastrichtian age which directly
overlies the weathered amphibole-bearing basalt. These
basal sediments, approximately 18 meters in thickness, havean irregular laminated structure and contain an impoverished assemblage of calcareous nannofossils and benthonicforaminifera. No palynomorphs have been found. Several
thin (<l cm) layers of apparently volcanogenic sand are
distributed irregularly throughout the section.
A fresh diabase sill, 10 meters in thickness, has intruded
the sediments 18 meters above basalt. Core recovery in the
intruded sediments was poor, but they appear to vary fromtypical nonfossiliferous iron- and pyrite-rich deep-sea clays
above to iron-rich nannofossil ooze below the sill. The
mineralization of this unit may be related to the intrusionof the diabase.
Overlying the brown clay unit, at a sediment depth ofabout 300 meters, a series of micaceous silts and sands
appears. These terrigenous sediments, interbedded withvarying amounts of siliceous ooze, constitute a Pliocene
sedimentary unit about 200 meters in thickness. The
quartzose and feldspathic sands and silts contain abundantmuscovite, biotite, and chlorite with a heavy mineral suite
dominated by hornblende, epidote, garnet, tourmaline,
sillimanite, and pyroxene. The mineralogy is suggestive of acontinental provenance with a variety of rock types
including granites, metamorphics, and volcanics. It isconsistent with the sediments having been part of the
Nicobar Fan during Pliocene times, as is the presence ofreworked foraminifera of shallow-water origin. If theterrigenous sands and silts described above are indeed partof the Nicobar Fan and derived from the Ganges
Brahmaputra effluent, then reason for the cessation of
turbidite activity in the area within the Pliocene must besought. The isolation from turbidite deposition could havebeen caused by damming to the north, which may havearisen by the closing of one of the gaps in the Ninetyeast
Ridge against the Indonesian trench system. Alternatively,
the formation of the pretrench rise associated with bucklingof the Indian Plate as it descends into the Sunda trench
could be the reason for the absence of turbidites.
The uppermost 100 meters of Site 211 consists of upper
Pliocene to Quaternary radiolarian and diatom ooze withash beds. This pelagic sediment represents oceanic
deposition below the carbonate compensation depth. The
ash deposits are of rhyolitic composition and mostprobably have come from the volcanically active Indonesianarc system to the north. As far as it can be deduced fromthe incomplete core recovery at this site, ash first appears inthese sediments in the late Pliocene and may reflect onsetof arc-type vulcanism at this time. On the other hand, thesediments may merely mark a shift of the oceanic crust into
the proximity of the Indonesian arc during late Tertiary.
Magnetic anomalies 29 through the beginning of 33
trending east-west have been identified south of the Sunda
Trench some 250 km N20°W of Site 211 (Sclater andFisher, in preparation). These anomalies give a north-south
spreading rate of 6 cm/yr. Assuming the same spreading
rate of 6 cm/yr southwards from the beginning of anomaly
33 to the drilling site the age of oceanic crust in this area isestimated at 81 m.y. using the magnetic time scale ofHeirtzler et al., 1968. This is close to the early to middle
Campanian age (72 to 80 m.y.) of the sediments
immediately above the basement.
REFERENCES
Heirtzler, J. R., Dickson, G. O., Herron, E. M., Pitman, III,
W. C, and LePichon, X., 1968. Marine magnetic
anomalies, geomagnetic field reversals, and motions of
the ocean floor and continents: J. Geophys. Res., v. 73,
p. 2119.
Sclater, J. G. and Fisher, R. L., in preparation. The
evolution of the East Central Indian Ocean withemphasis on tectonic setting of Ninetyeast Ridge.

21CorelCored Interval .0-9 m

Core 2

Cored Interval :9-18 in

LITHOLOGIC DESCRIPTION

10YR4/4
2.5Y6/2
and
5YR3/2
2.5Y4/2

LITHOLOGIC DESCRIPTION

DIATOM RICH CLAY
DIATOM OOZECLAY RICH DIATOM OOZE
dark grayish brown
Diatoms
Clay
Spicules
ASH RICH DIATOM OOZE
olive gray
Diatoms
Rhyolitic Glass
SpiculesRads
FeldsparCLAY RICH RAD DIATOM OOZE
5Y5/1

50%
25%
15%

50%
25%
20%
4%

IX

5Y4/1
5Y6/2

2.5Y6/2

RAp RICH

mottled
5Y5/1
andCLAY SPONGE 5PICULE RAD RICH
DIATOM OOZE
olive and dark olive
Diatoms
60%
Rads: Spicules
Silicoflag.
Clay
1<B

2.5Y4/2
with 2.5Y4/0
and 2.5Y6/0

pumice fragments

5Y2.5/2
5Y6/1 to2.5Y4/0

5Y6/2
α A Y

Clay
65%
Rads
15%
Diatoms
10%
Spicules5%
Silicoflag.
1%
Glass (green and clear) 3%
FeOxideIX
COARSE ASH

CLAY RICH SPONGE SPICULE

5Y5/1

2.5Y7/0

CLAY and RAD RICH DIATOM OOZE
l i g h t graygranule-size
pieces of consolidated ash

5Y5/2
5Y8/2
5Y4/2

RAD RICH CLAY
ASH
white

5Y5/1

BΔD and ASH RICH DIATOM OOZE

olive
Diatoms
45%
Rads
35%
Spicules and silicoflag. 5%
Clay
15%

dark gray brown with mottles
and streaks of dark gray
Diatoms
40%
Spicules
25%
Cl ay
20%
Rads
10%
Silicoflag.
5%

2.5Y4/2
with 2.5Y4/0
and 2.5Y6/0

CLAY and RAD RICH DIATOM OOZE

2.5Y5/0
5Y4/2
streaked with

CLAY RICH RAD DIATOM OOZERAD and ASH RICH DIATOM OOZE

5Y2.5/1___5Y6/2
5Y4/2

IIXI5Y5/0
5Y5/2

CLAY and RAD RICH DIATOM OOZEt h i n deformed ash layers with
90% s i l t and sand size glass.__5_Y_6/2
5Y3/2

X-ray a t 8.40 m Quar 30, Feld 2, Plag 8, Kaol 7,
Mica 28, Chio 2, Mont 24

Explanatory notes i n Chapter 1

Explanatory notes in Chapter 1

ASH RICH DIATOM OOZESite 211

Hole

Core 3

Cored Interval:57-66 m

Cored Interval:95-104.5 m

FOSSILCHARACTERFOSSILCHARACTER
LITHOLOGIC DESCRIPTION

LITHOLOGIC DESCRIPTION

0.55Y4/1

to-1

Greenish gray
5GY6/1 with mottles
and streaks o f
5G2/1 and 5Y5/6
greenish black andl i g h t o l i v e brown

SPONGE SPICULES DIATOM RICH CLAY
Clay and clay aggregates 63%
Di
Diatoms
15**
Spicules15%
Ash (rhyolitic)
1*
Silicoflag.
λ%
3*
Rads
2%
FeOxide and opaques

-45
-85
120

5GY4/1

graded slightly
sharp contacts
SILI layer"TOGY5/2 grayish
green with
5Y7/2 yellowish
gray mottles ofash 5Y4/1-25

o l i v e gray to dark greenish
Feldspar (mostly K-sparrare m i c r o c l i n e ,sodic Plagioclase
Mica
Quartz
Clay
Sericite
Heavy minerals
CalciteRAD SPICULE RICH CLAY
(50-90 cm, Section 2)
sand mottles 90-110 cm, Section 2s i l t mottles
t r a n s i t i o n a l to

5Y4/1

CLAY with mottles of CLAYEY SILT
and layers of greenish RAD RICH
CLAY
X-ray at 97.20 m Quar 26, Feld 5, Plag 10, Kaol 3,
Mica 38, Chio 2, Mont 16CoreCatcher

SPICULE RICH RAD DIATOM OOZE
Diatoms4
Rads
3
Spicules1
Clay
1
FeOxide and opaques

5Y5/2-7/2
l i g h t o l i v e grayto yellowish grayCore
Catcher
X-ray at 57.90

R h y o l i t i c glass shards
Diatoms
Clay
Quartz, Feldspar,
Heavy minerals

Explanatory notes in Chapter 1

55-95X
0-15%
0-25«
<5%

Quar 2 4 , Feld 4 , Plag 1 1 , Kaol 5,
Mica 27, Chio 3 , Mont 26

Explanatory notes in Chapter 1

HSite211

Hole

Coreδ

Cored Interval :133-142.5 m

Coreδ

FOSSILCHARACTER

Cored Interval; 180.5-190

FOSSILCHARACTER
LITHOLOGIC DESCRIPTION

LITHOLOGIC DESCRIPTION

5Y2/1

SANDY SILT
olive black

0 . 5 - -_-_-_-_-_-_-_5Y5/2 lightolive graystreaked with
N4 medium darkgray

RAD CLAY
l i g h t brown

5Y5/2

CLAY RAD OOZE TO RAD RICH CLAYl i g h t o l i v e gray occasionalmottles o f dark gray (N3)
hard layers
54-59, 90-94 cm
Rads
56% Clay 80%
Clay
40% Rads 20%
Heavy minerals 2%
R h y o l i t i c glass 1%
FeOxide'1%

10GY7/2 paleyellowish green

PHILLIPSITE BEARING CLAY
Clay
Rads
Phillipsite
SpiculesFeOxide

85%
5%
6%
3%
1%

RAD CLAY
Cl ay
Rads

73%
25%

Other siliceous fossils 2%
5Y5/2
and
N3

N4 streakedwith 5GY5/2

CLAY RICH RAD OOZE
l i g h t o l i v e gray ooze badly
mixed up with dark gray radbearing f i n e sand, possibly
former injected around l a t t e r

5Y5/2

RAD BEARING SILT
Feldspar (orthoclase)
63%
Clay
16%
Mica
15%
Rads
5%
Heavy minerals - horn1%
blende, opaque,epidoteClayRads

a l t e r n a t i n g ClAYFY STIT - SILTY
CLΔY and SILTY SAND, very f i n e f i n e , may be d r i l l i n g a r t i f a c t injection of softer s i l t aroundbroken up sandier beds

dusky yellow green RAD OOZE
X-ray a t 141.20

Quar 23, Feld 4, Plag 10, Kaol 13,
Mica 10, Mont 40
5Y7/2 yellowish
gray mottled andstreaked with
5Y4/1 olive gray

g_AY RAD OOZEDJΛ*j**Other siliceous fossils
Volcanic glass

erw
*«
4%
Tr.

X-ray at 189.10 m Quar 13, Feld 4 , Plag 12, Kaol 12,
Mica 9, Mont 50
5Y5/2

pumice pebbles

Explanatory notes in Chapter 1

CLAY RICH RAD OOZE
Rads
Clay
Diatoms
Glass
Silicoflag.

75%
15%
5%
3%
2%

Explanatory notes in Chapter 1

LITHOLOGYPLIOCENE

2
0.5-

VOID

F

R

1
1
1

!
1
!
1 -124
1

1.0-

G

R

Hole
FOSSILCHARACTER

Core 9

Cored Interval:294.5-304 m

LITHOLOGIC DESCRIPTION

LITHOLOGIC DESCRIPTION

S.I

1

7

DEFORMATION |LITHO.SAMPLE |I

Site 211

Cored Interval:228-237.5 m

METERSCHΛSECTION

ZONE

AGE

_J

Core 7F )SSIrLRAC ER

5GY4/1
dark greenish
" **

Core
Catcher

CLAYEY SILT - very watery, liner
only partially filled
Feldspar
68*
M1ca
10%
Clay
30%
Heavy minerals
2%
SANDY SILT - sand fine grain size,
micaceous, some fragments silty
clay
Feldspar
68%
Clay
20%
Mica
10%
Heavy minerals
2%
SILTY SAND - abundant fragmentsof silty clay.
In base of Section 1 roundedfragments of CALCAREOUS SILTSTONE - probably once part ofindurated layer.
Calcite cement
65%
Feldspar
28%
Mica
5%
Heavy minerals
25!

1.0
SILTY CLAY with sand layers
medium dark gray

5Y4/1

R

M

1

R
N18
Maximum(F)

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

F

METERSFOSSILABUND.
PRES.
SECTIONZONE

AGE
PLIOCENE?

C ore
Cat cher

Explanatory notes in Chapter 1

LITHOLOGY

DEFORMATION |LITHO.SAMPLE |Cored I n t e r v a l . 2 5 6 . 5 - 2 6 6 m
FOSSILCH* RACTERCore
Catcher

LITHOLOGIC DESCRIPTION

Explanatory notes in Chapter 1
VOID
10YR5/4

CLAymoderate yellowish brown
-100

CC

5GY4/1SANDY CLAYEY SILT
FeldsparMica
Clay
Heavy minerals

68S!
10%
20%
2%

olive gray
Feldspar
80%
Mica
3%
Clay
15%
Heavy minerals of hornblende - epidote
2%
suite

Hole

CorelO

Cored Interval:389.5-398 m

Cored I n t e r v a l . - 3 4 2 - 3 5 1 n

FOSSILCHARACTERFOSSILCHARACTER
LITHOLOGIC DESCRIPTION

LITHOLOGIC DESCRIPTIONCore Catcher and Part of Section 1 contained:

Core Catcher Samples only
About 9 cm of s t i f f moderate brown (5YR3/4) clay richiron oxide. Also few small ( 1 x 3 cm) fragments ofhard bedded red and dark gray mineralized samples.
Three facies i d e n t i f i e d as follows:1) brown AMORPHOUS IRON OXIDE facies
Iron oxide
70%
Clay
20%
Heavy minerals, Feldspar,glass shards
10%2) dark gray PYRITE-RICH ASH facies
80% d e v i t r i f i e d glass shards o r i g i n a l l y ofbasaltic composition (clear rims with R.I.
>1.55) now almost t o t a l l y f i l l e d withbrown iron oxide. Few (1%) grains are
yel1ow-palagoni t i zed?
10% opaques - mostly p y r i t e , some cubes seen
9% micronodules - abundant minute iron oxide
grains scattered throughout
1% feldspar - some Plagioclase i d e n t i f i e d3) red ASH-Rl CH IRON OXIDE fades
90% iron oxide aggregates several of which are
d e f i n i t e l y hematitic.
10% altered glass shards - much of FeO has
probably replaced glass shards as few pale
brown shards with FeO do remain - also FeO
aggregates occasionally s t i l l have clear
isotropic rim.
Tr. feldspar
Tr. crystoballite (?) aggregates

5YR4/4 moderate brown
3%
Quartz10%
Feldspar (2« plag.)1%
Mica
Heavy minerals (inc. amphibole)
1%
Clay minerals
85%2) OAT
10YR2/2 dusky yellowish brown
Feldspar
9%
U
Mica
75%
Clay minerals
Iron aggregates
15%
Rads and fish remains
Tr.
3) SILTY SAND
5Y4/1 olive gray, believed to be cavings fromup hole.
X-ray a t 351.00 m Quar 1 6 , Feld 8 , Plag 2 , Kaol 2 1 ,Mica 8 , Chio 1 , Mont 42

X-ray at 398

Core
CatcherCore
Catcher

Explanatory notes in Chapter 1

Explanatory notes in Chapter 1

Quar 13, Feld 36, Kaol 2, Mica 13,
Chio 1, Mont 15, Paly 17, Hema 4

F
R

c
c

P
M

Core
Catcher.*••» .y.',V

-124
-140
-149
-10
-27

5R3/4 dusky red
5YR6/41O

D o l o m i t e

r h o m b s

"Z ü
n

T"_l_

p

CatcherThin Sections

Plagioclase (andesine-labradorite An.,6-53
sodic plag. <An 3 0 )Clinopyrox. - as above
Heavy minerals (hematite, magnetite)
Mica
Chlorite
Glass
Palagonite
Calcite

39%
25%
10%
2%
5%
1%
8%
10%

X-ray a t 409.10 m Calc 34, Quar 8, Feld 12, Kaol < l ,Mica 5, Chio 1 , Mont 2, Paly 38
X-ray at 411.80 m Calc 35, Quar 15, Feld 29, Mica 14,
Hema 7
X-ray at 411.90 m Calc 8 1 , Quar 5, Feld 7, Mica 7

Explanatory notes in Chapter 1

•

16.
^120
127

MICARB RICH NANNO OOZE
Variegated red (10R6/6), cream(10YR8/2) and gray (5Y4/1) l a t t e r predominant.
Nannos70-80%
Micarb
10-15%
Feldspar5%
Heavy minerals
2%
Do!omi te rhombs
1%
Hematite grains ~20u more common
in red layers
Sand
50%
Silt
50%
Brown (10YR5/4) layers < 4 mm
t h i c k at 59, 95, 97, and 98 cm.
60% volcanic glass strongly
altered with some i n c i p i e n t
Plagioclase and palagonite;
20% heavy minerals - goethiteor limonite aggregates, somehematite
Feldspar8%
Nannos10%
Mica2%

dusky yellow brown

Section 2, 114 cm HYPOCRYSTALLINE APHANITIC ROCK with

_1_~ L~—1— J —i—.^ | 1.

< U

Section 1 . 143 cm HOLOCRYSTALLINE PHANERITIC ROCK
with subophitic texture
Plagioclase (sodic plag. <An 3 0 c a l c i canijlesine A n µ β - 5 0 )55%
Clinopyroxene - purplish augite
20%
Heavy minerals
6%Mica (brown b i o t i t e )itChlorite8%
Zeol i te
2%
Amphibole
λ%Sericite3%
Epidote
1%

5'

2
N

LITHOLOGIC OESCRIPTION

VOID

0.5_

YR7/4 gradational l i g h t brown to gray orange

10YR2/2
5YR6/4 and 10YR7/4
10YR2/2[ LITHO.SAM

M
P

LITHOLOGY

1 DEFORMAT ION

cc

SECTIO,PMETERS| PRES.

Cl

Alterations of NANNO RICH CLAY
and CLAY NANNO OOZE
gradational contacts,
iron r i c h below andesite
f i n e r grained
Nannos10-50%("basaltic")
Feldspar1- 3%
5Y5/2 Weathered zone^
minerals
^ U

ll 1

itral
N

C

N

R

£

N

| AßUND.

AGE

SE

5GY2/1-i-[ FOSSIL

IAN
trifi dus

EARL Y MAE

z

2

S

Cored I n t e r v a l : H8.5-428 m"ANDESITIC" S i l l (Diabase)greenish black uniform composition
see below

1.0--Core 13VOID

Λ > V • ",**<.'-

1o

LATI: CAM

LITHOLOGIC DESCRIPTION

0.5-

g

Hole
FOSSILCHARACTER

1 1 1

_

1 DEFORMATMETERSPRES.

FOSSIL| AßUND.

ZONE

AGE
1

o

LITHOLOGY

Site 211|

Cored In t e r v a l : 09-418.5 m

Core 12FOSSILCHARACTERI

Hole[ LITHO.SAM

Site 211

Bedding: 1 to 5 mm t h i c k , many
beds have wavy (rippled?) contacts.
some beds l o c a l l y erode thosebelow, microfaulting i n places,
some mottles and a burrow i n
40-50 cm i n t e r v a l .
X-ray a t 418.60 m Calc 33, Quar 9, Feld 15, Mica 4 ,Mont 10, Paly 28
X-ray a t 419.50 m Calc 35, Quar 6, Feld 6, Mica 6,
Paly 47

Explanatory notes in Chapter 1to00

Cored Interval:437.5-447 m

Cored Interval:428-437.5 m

on
HW

FOSSILCHARACTERFOSSILCHARACTER

LITHOLOGIC DESCRIPTION

LITHOLOGIC DESCRIPTION

CLAY RICH NANNO OOZE and NANNO CLAY laminated
10R6/6 moderate
10YR2/2 dusky yellowish brownyellowish orange
Clay
NannosNannos72%
Clay
Feldspar10%
Feldspar10%
Dolomite10%
Dolomite
Heavy minerals
3%

BASALT flow
aphanitic, glassy matrix
partially palagonitized,
sporadic large amygdales
palagonitized crust mixed
with calcite

Two beds of moderate brown 5YR5/6 nanno clay indicatedactual contact lost in coring
BASALT weathered pillow lava
Texture varies from aphanitic to phaneritic veins (1-3 mm)
and amygdales of calcite common - some shown on log tol e f t also indicated in same way are patches of palagonitized glass
Phaneritic
60- 90 cm
Amygdaloidal Zone
60-102 cm
Aphanitic Zone (very fine) 105-120 cm
Aphanitic (fine)120-150 cm (Section 2)
0- 50 cm (Section 3)

polygonal outline (chilledcontact of flow?) of weatheredmaterial may be palagonite
palagonitized crust, calcite,
and fresh glass
palagonitized crust (chilled
margin?) with veins of calcite
in centeraphanitic becomingcoarser downwards

glassy groundmass

Core
Catcherpalagonitized zone

5 cm fragment o f
baked limestone
w i t h fragments o f
black glass andpale brown p a l a g o n i t eembedded i n i t

calcite veinslarge amygdales (<3 mm) phaneritic zone
calcite veinaphanitic
highly weatheredcalcite vein

Thin Sections
Section 2 , 60 cm PHANERITIC BASALT: h y a l o p i l i t i c
texturePlagioclase (An^-Anss) a n d albitized
Plagioclase
48%
Altered pyroxene
10%Titanomagnetite and hematite
8%
Olivine ghosts
5%
Calcite8%
Dark mesostasis
10%
Volcanic glass and palagonite
10%
ZeoliteCore Catcher, 1 cm APHANITIC BASALT: variolitic
texturePlagioclase laths (radiating clusters)
Dark mesostasis
Cryptocrystalline aggregates of devit.
glass
Olivine crystal outlines altered into
1ddings1te
Hematite, t i t a n o m a g n e t i t e
Volcanic glass
Palagonite

30%
20%
10%
5%
15%
15%
5%

X-ray a t 428.10 m Calc 3, Dolo 6 , Quar 1 3 , Feld 9 ,Paly 69

Explanatory notes in Chapter 1

palagonitized zone - incipient
crystallization polygons seen

j * _

Core
Catchei
Explanatory notes in Chapter 1

calcite and palagonite
large amygdales andpatches of calcite

phaneritic zone

highly weatheredcalcite veins 2-4 mm

aphanitic zone

phaneritic zone

SITE 211

0 cm

— 25

— 50

75

100

125

150
211-1-1

211-1-2

211-1-3

211-1-4

211-1-5

211-1-6
29

SITE 211

0 cm

I—25

50

1—75

I—100

125

150

211-2-1
30

211-2-2

211-2-3

211-2-4

211-2-5

211-2-6

SITE 211

0 cm

25

50

75

—100

125

150

211-3-1

211-3-2

211-3-3

211-3-4

211-3-5

211-4-1
31

SITE 211

0 cm

25

50

75

100

125

150

211-4-2
32

211-4-3

211-5-1

211-5-2

211-5-3

211-5-4

SITE 211

211-5-5

211-5-6

211-6-1

211-6-2

211-6-3

211-6-4
33

SITE 211

0 cm

25

50

75

100

125

150

211-6-5
34

211-6-6

211-7-1

211-8-1

211-9-1

211-9-2

SITE 211

0 cm

25

50

75

—100

125

150
211-9-3

211-12-1

211-12-2

211-12-CC

211-13-1

211-14-1
35

SITE 211

0 cm

— 25

— 50

— 75

—100

—125

150
211-14-2
36

211-14-CC

211-15-1

211-15-2

211-15-3

211-15-4