LATE QUATERNARY GLACIAL HISTORY

OF EASTERN CONTINENTAL SLOPE OF THE GRAND BANKS

R Sc. IIonoum Thesis 1\Iarch 1975

Clem J. Benteau Department of Geology Dalhousie University Halifa..'<, Nova Scotia

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Author:

Title:

DEPARTMENT OF G(:OLOGY

DALHOUSIE UNIVERSITY HALIFAX, NOVA SCOTIA

CANADA B3H 4)1

DALHOUSIE UNIVERSITY, DEPARTMENT OF GEOLOGY

B.Sc. HONOURS THESIS

Clement J. Benteau

Late Quaternary Glacial History of eastern

continental slope of Grand Banks

Permission is herewith granted to the Department of Geology, · Dalhousie University to circulate and have copied for non-commercial purposes, at its discretion, the above title at the request of individuals or institut'ions. The quotation of data or conclusions in this thesis within 5 years of the date of completion is prohibited without the permission of the Department of Geology, Dalhousie University, or the author.

The author reserves other publication rights, and neither the thesis nor extensive extracts from it may be printed or otherwise reproduced without the authors written permission.

Signature of -at1Lhor S\lpU'\1\~

Copyright 197S

Table of Contents

1. Abstract 2. Introduction 3. l\Iethods 4. Stratigraphy 5. Biostratigraphy G. Dis cas s io.a. 7. Fig>.1res 8. References 8. App9ndix

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Fig. l

Fig. 2

Fig. n .:>

Fig. 4

Fig. 5

Fig. 6

Fig. 7

Fig. 8

Fig. 9

Map sh::>wing general location of cor0s. Rectangle outlines area of Fig. 2.

Detailed bathymetry and location of cores.

StrRtigraphy of cores.

Biogenic components of muds in 74-021-24.

Biogenic compon.ents of muds in 74-021-16.

Coiling directions of Q=_J?.~.chyclerma in 74-021-24.

Pelagic/benthonic forarn ratios in 74-021-24.

Detrital carbonate comp::>sition of cores (estimated from smear slides.)

Snmma1~y of core age interpretation.

l. Biogenic components o.f all smear slides.

2. Grain size analysis.

3, Detailed core descrlption sheets.

- 1 -

Two twelve metre piston cores were collected from intercanyon areas of

the continental slop•3 off the south-western Grand Banks in water depths of

1400 and 1600 metres. These are the first cores in this region (to the author's

knowledge) which completely penetrate the late \Visconsin glacial sediments

and th:_ls are of prlme importance in understanding the effects of glaciation

in this area. Study of the climatic indicator Gl2_2i1;_?ri_na_:Pa_9hycl_E?Sffi::_l: revealed

glacial turbidite sands bounded on either side by interstadial silty rnuds. The

partial penetration of a second sand body of one of the two cores may indicate

a second glacial period, The cores were subdivided into fo~r units, units A

and C representing interstadial periods (A being Holocen·e), Units Band D

rep resenting glacial pe :rlods.

Ic8 rafted p·3bbles are found through::mt both cores b.eing more abundant in

Unit B which represents the late Wisconsin glaciation. The p.ebbles are believed

to originate from the Labrador S:3a·or W.gstern Grand Banks areas and have boeen

associated with th0 Labrador current. The main Lau ren';ian ice sheet and Local

Newfo'..l.ndtand ice by-passed the area, followlng prevailing currents,

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Il\THODUCTION

Two twelve metre piston cores were collected from Jnter:;anyon areas on

the C·)ntinental slop·e off the s0uth-western Gra:1d Banks. The cDres contained

a sequence of interbedded muds and sands subdivided into four units, with only

three of the four units being visible in core 74-021-16. Core numh:n 74-021-24 0 0

was taken at 42 59.4' N, 51 39.6'W in about 1400 metres ofwater. Core 0 0

number 74-021-16 was taken a: 43 30. 7' N, 52 53.1' Win about 1600 metres

of water. Box cores were taken in th.e vicinity of both cores thus ·cleterrnJn~ng

S'.trficial sediments. Figure 1 shows the regional location of th.e cores while

r. I•,igure 2 shows more detailed bathymetry.

The p:upose of the study was to determine Late Quaternary glacial effects on

the continental slope off the Grand Banks.

'.) - (.) -

l\1ETHODS

Cores were split in pbs tic liners and the split. faces cleaned and described.

Ab•)ut 22 mt::!tres of core were described, centimeter by centimeter, with

the aid of about 100 sm3ar slides. Standard sieve and pip·ette techniques have

bean used for about 40 grain size analyses. Hewlett Packard desk top calculator

and plotter were used .for plotting aad statistical parameters· of grain size data.

All plots are append.ixed at the back. Biogenic data was estimated from smear

slides as wera sand, silt and clay ratios which ware used in early interpretations

of lithologies, grading, etc. A binocular microscope and household food colouring,

as a stain, were used in foramini.fera studies.

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STnAT1G TtAPHY

Th3 seqL13nce of lithologies is summarized in Figure 3. The cores C•)nsist

of fo~n· un1ts; a mud, unit A; a sand, untt B; a mud, uni.t C; and a sand, unit D.

Uni.t D was not penetrated by core 74-021-16. Diagenetic growth of dark iron

sulphide mottles is characteristic of both muddy units. The colour of the

sediment ranges from grayish-olive (10 Y 4/2) in the muds to olive-gray

(5 Y 4/1, 5 Y 5/2, 5 Y 6/1) in the sands.

At the top of core 74-021-24 a 3ilty mud grades .slightly over th-3 first metre

where it terminates with a sand bed (105-107 em.). The follmving 1. 8 metres

shows no grading until a second sand at a~Jout 3 metres~ Thi.s is underlaln by

a '1 em. silty sand a.ncl a::-1 additional 8 em, sand. The base of thi.s unit is taken

at 4. 2 metres, at the top of a metre thick massive sandy silt. The sand beds

of th1s tmi.t were charaderized by sharp ba;:;al contacts aiJ.d tr-ansitional tops.

The second unit ranges from 4. 2 metres to 7. 31 metres, consisting of interbedded

san.Js and sandy silt beds, varying in thickness from 3 to 40 ems. Both the lower

part of Unit A and this unit are characterized by the abundance of fragmented

bivalue shells. The shells are co:1tinU•JUS from :1 to 4. 5 metres and also occur

in. sand layers at 5.02 ancl 5.20 metres. The shells are fragmentary, and

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l\Ir. D. Davies of the Nova Scotia 1\Tuseum was nnab1e t.o identify any with

Jertainty. TIF:J co)ntacts of the lBcls tend to b3 shartJ both to() and b::>ttom.

Typically the beds follow a seq·~ence of sandy silt beds o·verlying sand beds.

However, sandy silt b.3ds overlain by a :3andy silt bed and sand beds 0verla.i.n

by a sand bed have been noted. Individual bt3da are m'3.l'k<Old by slight colour

changes and gradational bases.

Unit C resem~Jles unit A with thick, silty muds and occasional sand layers.

The first mud exi:ended to 8. 5 metres and was fonnd to fine slightly with depth,.

until it terminated at a 10 em. sand' layer. The second mncldy bed was found

to grade slightly, being coarser at the base. This bed extended to 10 metres.

The last m;~ddy b::d, separated from the previous one by a 5 em. sand,continued

to tln base of Unit C w·here it transitionally graded in:o a 2 nv3tre sand, unit D.

The two sand beds mentioned in unit C distinctively differed in a)pearance to

tlDse of unit A. The contacts at both the base and top were transitional with

the basal being more distinct. The beds themselves were made of incomplete

s;mcl silt lamina.

Unlt D, the sand bed at the base o£ the core, appeared massive. A layer of

l.Jivalue shells were observed close to the bJttom of the unit.

t' ~

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Throughout the core, pebbles were occasionally foand. In utlit A several

were located, the largest being 2 em. in rliameter. Pebbles in unit B were

larger and more frequent, the largest h3ing 5 em. in diameter and striated.

One bed at 6. 5 metres co:.1tn..i.ned a few smaller p·ebbles (2 to 5 mm.) scattered

througho\.lt the bed. Both unit C and D ·co:J.tained one pebble each with diameters

of l em. and 2 ems. respectively. Most of th·e peb~Jles are of quartzite and

rnetamorphic lithologies.

Core 74-021-16 followed the same ~equence of lE1its. However, unit D was not

penetrated. A number of differences within each unit were observed.

Unit A extended for 7 metres being separated from nnit B by a s~arp contact.

tlB sand beds of unit A have sharp bases ancl tra~1s itionat tops, wt1ile those of

unit B have sD.arp contac~:s. Sand don1inates the top half of untt B with each

bed showing distinctive grading becoming granular at the base. Bivalue snell

fragments were present in the upper part of unit B, concentrated in the sand

beds. They were not present in th;:dower part of unit A.

Unit C again resemb1ed unit A. However, sand beds were m::>re freqllent and

demonstrated the characteristic contacts. Other notable features of this core

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wero sand pods in a nmcldy h3d of uni.t A and a lump of red clay p:::esent in

sard bed of unit B. P8b:Jles were scarca throughout the C·Jre. Three pebbles

were foLmd in unit A, two in unit B (other than in one bod which contained several)

an:l unit C was void of pebbles.

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BIOS'fRATIGRAPHY

The p'lleontologic analysis of the sediment followed two linea. Through the use

of smear slides, estimates were made, d·31::ermining what percentage of the

sedim:mt was of biogenic origin. This included coccoliths, forams, diatoms

and sponge spicules. This is summarized in Figures 4 a_rld 5. A second study

was completed on the distribution of dextral and sinistral c.::>iling forms of the

Ratios of plan~-donic to benthonic foraminjfera were also determined. Thts is

summarized in Figures 5 and 6.

The clomtnant species of foraminifera in all sam~)les were Gl~?lgerina bL11loi9!3s

and Globigarina pacjly_il_~;rm,~-, with Globiger.ina bulloides_ dominant. Both forms

are p1.anktonic and characteristic of subarctic a.1d transitiona!_ water masses.

No changes of diversity or dominance were noted. Dextral forms of Glo!J~g~

.J2.:~<;:l:}ydaiP2.. are tolerant of higher temperatures than the sinistral and can thus

be used as a climatic indicator (Wollen et al, 1970). The climati.c curve, Figure 6,

demonstrates a cooling of th·8 water mass corresponding to units Band D with

wa1.·mer water on either sic1•3.

The distribution of coccoliths and total biogenics demonstrate a similar rela~ionshi.p

with marked incraases a!: both the lower limit of ulltt A and th3 upper limit of unit C

in b:>th cores.

Af'' ~

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DISCUSSION ·4-· ~------

Th3 mos~ obvioas cha.ra·::terlstic oi the slope of the Grand Ban~\:S and extenclin::;

to Cape Hatteras is the abundan::!e of snbma.rine canyons which have been the

pri.rne attention of marine geologists, finding them of greater lntereat than the

relatively featureless slopes. This leaves one with little knowledge of the

retative importance of the many mechanisms.providing sediment to the slope

environment. The possible sources of sediment to this area are from the

adjacent shelf and the Laurentian chann·el. The tramport and escape of

sediment from shelf areas its.elf involves a number of mechanisms, (Emery

and Uchupi, 1972; McCave, 1972). At the shelf break, turb'.llence results in

rv:1arly continuous sco:1r and resuspenston with measured amounts of susp·:msion

in the water mass being high cluring most of the year. Unstr2.tified shelf water

can scour sediments. and modify the sea floor as it cascades off the shelf often

obtaining a velocity o.f 10 em/sec an.d thus being capable of moving fine susp::mded

rnatet.'ial. Submarine canyons act as a sump to which suspended material moves.

Suspension of fine materi.at occurs through a mtmber of process8s including

periodic slump~3, disturbance of benthic organisms, internal brsa~-dng waves

an-:t storm induced turbc1lence. The upp2r slo;::J3 is typica:ly comprised of

alternating heels of mnddy silt and silty mud, usually highly bioturbated, (Piper

and Normark, in press). Coarser material is su.;>pliecl by splll over san.js giving

blanket graded sand .beds. Slumping may O·::!c•_tr leaving depressions which refill

with s8diment. Up;Jer slops depo3lts contain Le3s san,j than sh·3lf d•3posits. For

(

r

. - 10-

secUment deposited lower c'bwn on the slo,)·3, redistrlbutioi1 ot the sediment is

P•)Ssible thl'CJ;_lgh down-slope movemt'lnts (turbidity currents, slumps and ,

possibly, lutite flows), clisturbanc:e by benthic organisms and contoar currents,

S!.lC~l as the Western Bou1.dary Undercurrent. The effect o.!: this current on

th8 slope is not well und·3rstood although it probably affects water depths of

1500 metres and greater landward of th.;:: Gulf Stream. The southwestwa:r:d flow

of asso0iated Norwegian S.3a overflow water flows at a depth of IOOO metres

(Em9ry and Uchupi, 197:2). The sediments of the two cores have been influenced

by some or all of these processe;;;.

Occasio11al sand beds m~:mtioned in units A and C show characteristics o.!: turbidity

car:rent origin. Features such as sharp erosional bases, basal grading and

transitional tops grading into mud.s demonstrate thj_s. Internal stnwtures o£ tha

bed, such as cross stratification and parallel lamination.s are tmpossible to

determi.ne without the aid of X-racllographs. The m::>st likely source o£ the sand

is spillover deposits of the upp.er slops indicated by high concentrations of silt

and generally finer grain size than sand beds to be discussac! la':er in untt B

(Stanley, et al, 1972). A second typ·3 of density current that may be responsible

for depDsition of muddier material in units A and Care lutlte .flows (McCave, 1972).

However, these low velocity, low density turbidity currents wo~lld be imp·::>ssible

-11-

to detect. S1ump3 may occur on steep slopes ~nt since b.:::>th c.::n·es corralate,

th.;;r<J is no evidence of slump lo3ses. The abundance of silt in the muddy beds

of tmits A and C is tndica~ive of storm turbulen:;e a:: the shelf, bt3ing the only

m3chan5.s m available that coutd create the necessary velocities to suspend silt

Unit B consists of a series of interbedded sands and silts and correlates with

simJlar beds of the Scotian slop:3. The Scothm slope sand sequ3nce has been

interpreted by Piper, 1975, as marking the Late Wlscortsin staclia1. Presumably

" "l: i

this is true of the Grand B::nk3 slope beds as well. 'With the arJvance of the polar

ice. cap a lowering of sea lev·al woald oc.::mr, exposi.ng portions of the C·:::>ntino::mtal

terrace. This would enable river outwash and shora line features to prograde

seawarcls with resulting deposition of coarser material into previously deeper

water. This seaward movement is also evidenced by the existence of bivalue shelts '

in the upper part of this unit being displaced seawards with lowering of sea level.

The increa3ed dextral coiling of Globigerin~p::tchyderma indica~es cooling of the

water column during the dep::>sition of this unit. The mode of transp·::lrtation of

sediment to this area is somewhat ambiguous. The relative importance of down

slop8 tr<J.nsport by density current and straight. "diffusion'' is not dear. In core

74-021-16 the appearanc:e of well graded beds indicates turbidity current dep·:::>3its.

However, this is not as distinct in core 74-021-24,.

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Unit C highly resembles that of unit A and th2 processes involved are presumably

the sam.3. In core 7t1-021-2+ the two sand beds mentioned previously in the

stratigraphic section contain silt laminae that may b·3 interpreted either as

bottom current deposits or at:; turbidity current cleposits. Howevar, a turbidity

current origin seems mora probably on the b:1sis of sorting a~1d bedding structures.

Unit D, present in core 74-021-2-± only, either ma:eks a sec.:md glaciation or an

abandoned su~)marine c~1an.,1el, or both. The former seemG more probable due to

increase of grain size and presence of bivalue shells in the lower part of the u:a.it.

It is further supported by one foraminiferal a_1alysis indicating cooling. A further

Ice rafting contributes unkn~nvn amounts of detrital ms.terial. to the cores, since onty

the coa.r.se fraction ca'1 demonstrably be rafted. The greater abun~ance of raf~ed

' peb~Jles in core 74-021-24 compared to 74-021-16 suggests selective movem:mt of

hergs from the vVisconsin ice sheet. As stated by Piper (1975), Laurentian Channel

ice movas west as it leaves the chann9l, carried by prevatling currents. This is

presumably true of Western Grand Bank ice a3 well. The sourca of rafted p9b~les

theret"ore originates from the eastern Grand Banks or Labrador S·3a) carried by

prevoJli.ng currents, as well as th·3 Labrador current. Thus, only bergs escaping

from the current would ha;re rea.Jhed the location of core 74-021-16 which is walt

-- 13 -

protected by the tip of th3 Gr;md Banks. The source of the bargs is well

s·Jp;Jorted by the petrology o.f the gravel.

Th-3 sands of unit B tend to be primarily composed of quartz a~1d feldspar,

q nrtz dominating, la:;king any rock fragments. This indicates a mature source

from the Ban~-\:S with no outwash material from Newfoandland reaching this area.

S;;ods 0f the Nova s.:::otian slop·e are abundant in rock fragments. This suggests

a low sedimenta~ion rate on the Grand Ban~zs slope con1.;:Jared to the Nova Scotia

slo~·3 during glaciation.

Biogenic contributions to the sediment of pelagic ~icr?fossils (foraminiferas,

cocc.::>liths, diatoms) as well as sponge spicules c1omlnate in units A and C

with marked decreases in glacial u;1it B (Figs. 4 a~1d 5). This could be due to

changes in productivity or terrigenous sedimentation rate or hoth. !he blooms

of life both pre and post glaciation could possibly have been induced by more

frequent convection of the water column supplying consta_nt nutrients at the surface

as well as destroying pelagic populations. Higher organic eontrlb:.1tions have been

noticed in sand beds of both units A and C which are presumably of upper slope

where on would expect higher biogenic input dae to increased productivity a;1d

sedimentation rates. The decline or b.enthonic foraminifera in unit B is anomalous.

Thts' is a possible result of low productivity, unstable substrate or greater solutio:1

of tests in colder gladal waters. The latter \voul~l al.so effect total biogenic

- 14-

contrlbLttio;:l.S. Benthonic to planktonic ratios Rre SLtmmarlzed in Figure 6.

Pctrit.al carbonate, sammarized in Figure 7, shows a similar trend with

marked decreases in unit B. Thi.s may be to some ·extent an indication of

greater solution. The two possible sources of detrital carbonate being the

Grand Banl<:s and th8 Laurentian Channel. The Grand Bank is the likely

source for the majority of the carbonate suggested by high quantities in sands

(S1att, 1974). However, minor amounts may originate from the Laurt:mtian

Channel shown by a lump of red cl~y probably originating front the Laurentian

~ 1 Ch::mnel.

As mentioned previously, ratios of dextral to sinistral coiling of Glooigerlna

Q~g_l}Y.'i~~ were determined. This indicated a cooling of water during the

sedimentation of untt Bas well as a period of maximam warming probably

corresp·::mding to that of 4000 B. P. (The interval- Plink, 1956, p. 396). More

samples are needed to b-etter pin point this ma.'dma. '

In su.mmary, the cores represent two glacial periods, units Band D with

accompanied interstadials u.aits A and C. A s:3a level lo-.vering of about 90 metres

is 1Beded to give a 3teep 3Ubmarina gradient immediately offshore from the coast

L ~ tha.t is n8ec1ecl to produce turbidity m1rrents on the continenta'. slope. Thus,

- lG -

extrapolating frorn a .3Ul'ile of wa~er clopth to time (Em:=ny and Uch~1pi, 1972),

+ c8Jl give an approximate elate to the top of glacial unit Bas 11000 B. P. - 2·)00

years. Also using sea level cu:cves of Bloom et al, 1974, which show good

cor.rela'.:ion with Dreimanis and Kar.row's, 1972. Ontarlo ice advances,

(i.e. Laurentide ice) approximate dates may ba given to major sea level

fluctuations. This is reasonable since flu~tuations of Laurentide ice is of

prime imp:::>rtanca in C•)ntrolling sea level. This also supports the date for the

top of unit B provided from Emery and Uchupi 's data. One can~now correlate th-')

base of unit B to th-9 date of the rapid end of the Plum Point interstadial in

("' .. i Ontario at 22000 B. P. ± 2500 yaars. The top of unit D would thus correspond

to the Cherry Tree stadial ending 36000 B. P. !: 3000 years. This is summarized

on Figure 9. One can now make inferences on relative rates of sedimentation.

This gives a valu·3 of 40 to 60 cm/1000 years for untt A. This is somewhat

· an-::>malous being higher than that of glacial un.i.t B knowing the rate of sediment

S:.lpply to the Grand Banks during interstadial unit A being minimal evidenced

by reliet deposits of the banks descrlbad by Slatt (1974). Biogenic contributions

nnst highly support the rate of sedimentatlo:1. This is SLlpported by Figures 4 ·

and 5, s'n0wing r.Li.gher biogenic inpat during interstadial times. This is presu. .. '1.1ably

tru8 of interstadial unit C as well as showing similar biogenic comp:::>llents.

S3climentation rates of unUs Band C are 30 to 40 cm/1000 years and 25 to 30cm/

lOOCl years resp•3ctively.

HE J'EHENCES

· l. Bloom, A. L.; Broecker, W. S.; Chappel, J. 1\L A.; 1\Iathew.s, R. K.; an.d J\Icsolella, K. J.; 1974. Qua~ernary Sea Lev0l Fluctuations on a Tectonic Coast: New 230 Th (231 U Dates from the Huon Penin::mla, New Guinea QLtaternary Res:::Jarch 4, 185-205.)

2. Dreimanis, A. and Karrow, P. F., 1972, Glacial History of the Great Lakes St. I.awrence Region, the Classification of the \Visconsin (an) S~age and Its Correlatives, 24 LG.C., 1972, section 12.

3. Emery, K. 0. and Uchupi, E. 1972 Western North Atlantic Ocean: Topography, Rocks, Structure, Water, Life and S·3dlments. American Association of Petroleum Geologists, Memoir 17.

4. Flink, R. F., 1956. Glacial and Pleistoeene Geology, N. Y.

5. McCave, I. N., 1972, Transport .and Escap·3 of Fine-Grained Sediment from Shelf Areas. In Swift, D. J. P.; Duane, D. B.; and Pilkey, 0. H.; et al. s:1elf S.3cUmcmt Transport, Stroudsburg, Pa., p. 255 - 248.

6. Olsson, R. K., 1974. Pleistocene Paleoceanography ~md Globigerlna Pachyderma (EHRENBERG) In mte 36, DSDP, Northern Pacific Journal of Foraminiferal Hes:3arch, v. 4, no. 2, p. 47-60, pls. 1-3.

7. Piper, D. J. W., 1975, Late Quaternary Deep Water Sedimentation off Nova Scotia and Western Grand Ba...nks. In print.

8. Pip·3r, D. J. W. and Normark, W. R., 1975 The llioDell Formation: A Plio~ene Continental Slope Deposit in Northern California. In Print.

9. Slatt, H. M., 1974. Continental Shelf S:3dimen~s off Eastern Newfomtdland: A Preliminary Investigation, Canadian J::mrnal of Earth Sciencea, 11, 362.

10. Stanley, D. J.; Swift, D. J. P.; Silverberg, N.; James, N. P.; and Sutton, R. G., 1972. Late Quatenw.ry Progradation a...11.d Sand Spillover on the Outer Continental l\hrgin off Nova Scotia, Southeast Canada. Smuts on. Contribution to Earth Sciences, 8, 88p.

ll.

( I \:j~ ...

W·ollin, G.; Ericson, D. B.; and Ewing, l\1.; 19 Late Pleistocan8 Climates Recorcled in Atlantic and Pacific Deep Sea Sedime1its, 1970. Science v. 1G7, p. 1483.

LABRADOR~S£A

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