Main Lithologies and Preliminary Interpretation of ARK-XX/3 Sediment Cores

R. Stein

During the „Polarstern“ Cruise ARK-XX/3, sediment cores were taken at 26 sta-tions in total (see Chapter 9.4 for details). In the following, the main lithologies of the recovered sediments are described and preliminary interpretations are given. The detailed lithological core descriptions are presented in Chapter 12.3 of the Annex.

Lithostratigraphy of sediment cores from the Svalbard continental margin and eastern slope of the Yermak Plateau

One of the main targets of the ARK-XX/3 geology program is the study of sedi-ment dynamics of mega-slides along the Svalbard continental margin (as part of the ESF Program „EUROMARGINS“) (Fig. 9.30). In this context, the characteri-zation of sediment facies within debris flow and turbidite sequences as well as undisturbed (hemi-) pelagic sequences, the dating of sediment mass flows, and estimates of sedimentary budgets are of interest. In order to sample sedimen-tary sequences within the mega-slide area as well as the adjacent undisturbed (hemi-) pelagic facies, detailed PARASOUND and Hydrosweep surveys have been carried out (see Chapters 7 and 9.2) to select optimum coring stations. At the southwestern flank of the mega-slide area, several couples of sediment cores representing slide-influenced facies and (hemi-) pelagic facies were taken (Fig. 9.31).

Fig. 9.30: Assumed extension of the mega-slide („Yermak Slide“) area north of Svalbard (light gray area in the left figure) (Figure taken from ESF-EUROMARGINS proposal on „Slope Stabil-ity on Europe’s Passive Continental Margins“, coordinated by J. Mienert, Tromsø UniversStabil-ity,

Fig. 9.31: PARASOUND profile and locations of cores PS66/306 to PS66/309 as an example for the sampling strategy. Cores PS66/306 and PS66/307 were taken inside the slide area, PS66/309 at the marginal part, and PS66/308 in the (hemi-) pelagic facies outside the slide area.

A key core within our research will be Kastenlot Core PS66/309-1 obtained close to the edge of the mega slide (Fig. 9.31). This core is composed of very different lithologies as shown in Figure 9.32 (for detailed lithological core de-scription see Chapter 12.3, Annex). Based on sediment colour and texture, the sequence can be divided into nine units. Unit I (0 to 61 cm) is composed of brown and very dark brown silty clay with some layers of mud clasts. Under-neath an about 20 cm thick interval of dark gray to very dark gray silty clay is obvious (Unit II). Unit III (89 – 138 cm) is an olive brown, partly bioturbated silty clay. Unit IV (138 – 204 cm) and Unit VI (272 – 299 cm) consist of olive gray silty clay. Between these two units, an interval characterized by dark gray sandy silty clay and sand alternation and fining-upwards sequences (Unit V). This tur-bidite unit has a sharp (erosional?) contact to the underlying Unit VI. Unit VII (299 – 510 cm) is mainly composed of dark grayish brown, partly bioturbated silty clay with occasional occurrence of very dark gray layers and dropstones.

Unit VIII (510 – 641 cm) is characterized by alternation of olive/dark olive gray and dark gray/very dark gray (sandy) silty clay. The uppermost part of this unit is more coarse-grained, and at the bottom of this unit (636 – 641 cm) gray and dark olive brown beds occur. The lowermost unit (Unit IX; 641 – 765 cm) con-sists of dark gray to very dark gray silts clay.

Fig. 9.32: Major lithologies of Kastenlot Core PS66/309-1

The distinct changes in sediment colour (and grain size) in the record of Core PS66/309-1 may represent glacial/interglacial variability (with the dark gray/dark olive gray intervals such as the lower part of the sedimentary sequence proba-bly representing glacial and the brownish intervals probaproba-bly representing inter-glacial intervals; e.g., Jakobsson et al. 2000). The turdidite sequence (Unit V) is related to the mega-slide event. The turbidites occur in reduced thickness also

Main lithologies (units) of Core PS66/309-1 KAL

Brown, dark brown

Grayish brown, dark grayish brown, and olive brown

Gray, dark gray, very dark gray Olive gray, dark olive gray

Dominant sediment colours

Lithology Lithology Lithology Lithology Lithology

Turbidite sequence

Turbidite sequence

Turbidite

Lithostratigraphy ARKXX/3 Cores

Grey, dark grey, very dark grey Dominant sediment colours

Brown, dark brown Greyish brown, dark greyish brown and olive brown Olive grey, dark olive grey

ments under- and overlying the turbidite unit can be done, this gives the unique possibility to reconstruct the history of the mega-slide event at the northern Svalbard continental margin.

Similar lithologies as described for Core PS66/309-1 were also recorded in the other (pelagic) cores obtained in the study area during this cruise. Based on the lithological core description, a correlation between these cores is possible (Fig.

9.33). In general, this correlation is also supported by the wet bulk density and magnetic susceptibility reords (see Chapter 9.3.1, Figs. 9.11 and 9.12).

Fig. 9.33: Major lithologies of cores PS66/308-3, PS66/309-1, PS66/311-3, PS66/321, and PS66/329 (For core locations see Figure 9.1).

The lithology of Core PS66/325-3 taken from the continental slope north of North East Land at a water depth of 895 m, differs from those described above.

Except the uppermost dark brown-coloured silty clay, very dark gray and dark olive gray silty clay and sandy silty clay are the dominent type of sediment (Fig.

9.34; for details see Annex 12.3). The sedimentary sequence can be divided into six main lithological units. Unit I (0 to 10 cm) is composed of very dark brown silty clay with mud clasts in the lower part. Units II (10 – 230 cm), IV (274 – 516 cm) and VI (545 – 648 cm) consist of very dark gray to olive gray silty clay. In between these units, two more coarse-grained (sandy silty clay) units are intercalated: Unit III (230 – 274 cm) and Unit V (516 – 545 cm). The upper part of Unit V (516 – 524 cm) is a diamicton-type sediment. These two more coarse-grained units probably represent glacial stages. Furthermore intervals with significant amount of ice-rafted debris (IRD), especially in Units III and V, are obvious (Fig. 9.34). These pulses of maximum IRD input may be related to advances of the near-by Svalbard-Northern Barents Sea Icesheet, as described for Marine Isotope Stages (MIS) 6, 5d, 4, and 2 (e.g., Mangerud et al. 1996).

Fig. 9.34: Major lithologies (Units I to VI) and amount of ice-rafted debris (IRD) of Core PS66/325-3. Arrows indicate maxima in IRD input, probably related to fluctuations (advances) of the Svalbard-Northern Barents Sea Icesheet during glacial stages.

Future sedimentological, micropaleontological, and geochemical studies and, especially, the dating of the sediment cores are needed for more detailed inter-pretation in terms of paleoenvironmental history.

Sediments and rocks from the top of the central Yermak Plateau: Implications for basement origin?

As outlined in Chapter 8, it is assumed that the northeastern Yermak Plateau is oceanic in origin, while its southern part might consist of stretched continental crust. Thus, on top of the central Yermak Plateau where old strata (basement?) probably terminate close to the seafloor, the sediment dredge as well as the gi-ant box corer and the gravity corer was used for sampling at several stations (Fig. 9.35). The sampling stations were selected based on detailed PARA-SOUND and Hydrosweep profiling. Fur this purpose, steep slopes and peak elevations with lacking young soft sediments on top were of interest (Fig. 9.36).

Fig. 9.35: Stations of „basement sampling“ on top of the central Yermak Plateau

Fig. 9.36: PARASOUND and Hydrosweep profiles across the central part of the Yermak Pla-teau with sampling stations.

At the western steep slope (location PS66/335), huge amounts of stones have been dredged (Fig. 9.37; for exact dredge location see Table 9.3). The majority of stones is black-coloured/-coated. After cutting, however, a large number of stones were identified as red sandstones. At the same location, also a gravity core (PS66/335-2) was taken. In this core, only 32 cm of sediments were re-covered. Part of the recovered sequence is composed of – for this area – non-typical red-coloured sediments (Fig. 9.38).

PS66/337-4 PS66/337-3 PS66/336-3

PS66/336-1

PS66/335-2

Dredge PS66/335-1 540

520 500

560

B. Platten, R. Rathlau, A. Winkler

Dredge

Fig. 9.37: Dredged rocks at Station PS66/335, central Yermak Plateau

Fig. 9.38: Sediments recovered in gravity core PS66/335-2, central part of the Yermak Plateau

At sites PS66/337-3 and PS66/337-4 located in the eastern part of the profile (Fig. 9.36), no penetration with the gravity corer was possible. At Site PS66-337-3 the core catcher of the gravity corer even became damaged when hitting the hard “basement” rocks at the seafloor. In the core catcher of both cores, mainly black (basalt-like looking crystalline) stones or fragments of them were recovered.

Based on these very preliminary results and still speculative interpretation, the basement may have a continental origin (Devonian Old-Red sandstones?) at the western slope of the profile whereas in the eastern part basaltic material may be cropping out, indicating an oceanic origin. Of course, more detailed work on the petrology of the dredged material should be performed before a more precise interpretation about the basement origin of the Yermak Plateau in this area can be done.

Sediments from the East Greenland continental shelf: Pre-Quaternary base-ment and Quaternary paleoenvironbase-ment

As part of the IODP site survey, seismic profiling was carried out on the east Greenland shelf during this expedition (see Chapter 8). In this area, seismic data reveal the presence of a prominent salt province and suggest that Meso-zoic sediment are cropping out at the surface (Schmitz and Jokat, 2005). In or-der to sample these old strata, 10 gravity cores (using the short 3m core barrel) were taken. The location of the cores was selected based on PARASOUND profiling (Fig. 9.39). Based on comparison with the seismic profile, faulted old sediment strata and a salt diapir can also be assumed in the PARASOUND pro-file.

Fig. 9.39: PARASOUND profile and core locations, East Greenland Shelf (for location of area see Fig. 9.1).

In the southern part of the profile (PS66/343-1 to PS66/343-6), where pre-Quaternary (Mesozoic?) sediments should be sampled, unfortunately only soft (young) sediments were recovered (Fig. 9.40). Some of the gravity corers even over-penetrated into the seafloor. At Site PS66/345 located on top of the as-sumed salt diapir structure (Fig. 9.39), however, coring of old strata was suc-cessful. At Station PS66/345-2, a 1.5 m long gravity core was recovered (Fig.

9.41). In the lowermost part of the sequence(core catcher), small light gray

„crystals“ and one large white-orange „crystal“ of about 4 cm in diameter were found (Fig. 9.42-A). X-Ray analysis of the large „crystal“ indicates that it is pure gypsum (Fig. 9.42-B). This may suggest that the gravity corer may have hit the (Permian?) salt diapir surface (or came at least very close to it). This important finding may support the interpretation of the seismic data of Schmitz and Jokat (2005).

Fig. 9.40: Corer penetration and core recovery of gravity cores from the East Greenland Shelf.

3

2

1

0

PS66/343 -1 -2 -3

-4 -5 -6

-1 -2 -3 PS66/345

Penetration (m)

Recovery (m) Soft young sediments

Fig. 9.41: Lithology and preliminary interpretation (Core PS66/345-2, East Greenland Shelf)

Fig. 9.42: (A) Photograph of core catcher sediments recovered in gravity core PS66/345-2 (East Greenland shelf). Common small white rock fragments („crystals“) and one large „crystal“ of about 4 cm in diameter are obvious. (B) X-Ray diffractogram of the large crystal found in the core catcher, identified as gypsum (X-Ray analysis has been performed by Chr. Vogt, Bremen University).

The main part of the sedimentary record of Core PS345-2 that is certainly of Quaternary age can be divided into three main units (Fig. 9.41).

- Unit I (0 - 60 cm): soft brown to very dark grayish brown sandy silty clay - Unit II (60 - 83 cm): very dark grayish brown silty clay

- Unit III (83 – base): firm (overconsolidated) very dark gray sandy clay with abundant pebbles (diamicton)

From correlation with similar sequences from the East Greenland continental margin (e.g., Stein et al., 1993; Hubberten et al., 1995; Funder et al., 1999), these lithologies can be interpreted in terms of East Greenland glacial history.

The sediments of Unit III (a tillite) probably represent the Last Glacial Maximum (LGM) glacial advance. The site was overridden by glaciers as shown by over-consolidation. Overconsolidated sediments are also reflected in the shear-strength record (see Chapter 9.3.3, Fig. 9.15). The deglacial retreat of glaciers is documented in the sediments of Unit II. The uppermost Unit may represent the glacial-marine post-glacial (Holocene) time interval. Finally, it has to be mentioned that it cannot be excluded at this stage, that the diamicton of Unit III may be related to older (Marine Isotope Stage 6?) glaciations. AMS¹⁴C datings are needed to give a more precise interpretation of the sedimentary record of Core PS66/345.

Im Dokument Scientific Cruise Report of the (Seite 86-99)