facies analysis of the renmark group sediments intersected ... · detailed analysis of the...
TRANSCRIPT
6Hi<v CoHflJC(lAs e.'t
Department of Primary Industries & Energy
BUREAU OF MINERAL RESOURCES, GEOLOGY & GEOPHYSICS
RECORD 1990/2
Groundwater Series No. 19
FACIES ANALYSIS OF THE RENMARK GROUP
SEDIMENTS INTERSECTED IN WOODLANDS 1
MURRAY BASIN
(NSW Department of Water Resources Bore No. 36670) (BMR ANABRANCH 3)
by
Robert Langford
(Graduate Student, Australian National University, Canberra)
Produced as a contribution to the joint Commonwealth and States Murray-Darling Basin Hydrogeological Project
The information contained in this record may not be published in any form or used in any company prospectus or statement without the permission in writing of the Director,
lJureau of Mineral Resources, Geology and Geophysics.
IIII *R9000201*
CONTENTS
ABSTRACT .............................................. 1
INTRODUCTION . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .. 1
GEOLOGICAL SETTING ................................... .. 1
LITHOFACIES ........................................... .3
GENERAL DESCRIPTION ............................... .. 3
LITHOFACIES A: GLAUCONITIC SAND ........................ 3
LITHOFACIES Bl: BIOTURBATED SAND AND SILT ................ 9
LITHOFACIES B2: SAND AND SILT ........................... 9
LITHOFACIES B3: COARSE SAND AND SILT ..................... 9 LITHOFACIES C1: SAND DOMINANT .......................... 20
LITHOFACIES C2: SAND DOMINANT .......................... 20
LITHOFACIES C3: SAND DOMINANT .......................... 20
LITHOFACIES D: SILT DOMINANT ........................... 21
DIAGENESIS ............................................. 21
DISCUSSION ............................................. 21
ACKNOWLEDGEMENTS ..................................... .23
REFERENCES ............................................ 23
TABLE
Table 1 Lithofacies and interpreted depositional environment ..............23
FIGURES
Fig. 1 Locality map .......................................2
Fig. 2 Framework tectonic elements and underlying infrabasins . . . . . . . . . . . . .. 2
Fig. 3 Cainozoic stratigraphy of the Murray Basin . . . . . . . . . . . . . . . . . . . . . .3
Fig. 4 Woodlands No 1 stratigraphy ............................. .4
Fig. 5 Structure contours on the base of the Renmark Group, Murray Basin ..... .5
Fig. 6 Lithostratigraphic column of Woodlands No 1 .................... 6
Fig. 7 Sedimentary features of the Renmark Group . . . . . . . . . . . . . . . . . . . . .7
Fig. 8 Biological properties of the Renmark Group .................... 8
Fig. 9 Schematic reconstruction of depositional environments ............. .22
PLATES
Plate 1 Lithofacies A and Bl .................................. 11
Plate 2 Lithofacies B2 and B3 ................................. 13
Plate 3 Lithofacies Cl, C2 and C3 .............................. 15
Plate 4 Lithofacies D ...................................... 17
Plate 5 SEM photographs of clay minerals ....................... .. 19
APPENDICES
Appendix 1 Detailed logs of the Renmark Group sediments .............. .25
Appendix 2 Clay analyses . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . ... 35
III
1
ABSTRACT
Sediments of the Renmark Group intersected in BMR Woodlands No.1, in the Murray Basin, NSW, represent part of a southward directed fluvio-Iacustrine system. The unit consist of approximately 150 metres of interbedded fine to coarse-grained sands and carbonaceous, laminated fine-grained sands and muds.
Detailed analysis of the sediments has provided information for determining the depositional and stratigraphic character of the unit. Four lithofacies A, B, C and D are differentiated on lithological, sedimentary structure and biological properties. Two of these facies have been further devided into subsets i.e. Bt, B2, B3 and Cl, C2, C3.
Within the sand lithofacies specific environments have been recognised, including meander channel point bars and levee deposits, as well as crevasse splay sequences. The laminated facies represent lake, well to poorly-drained swamps and paralic mudflat environments.
The lower part of the sampled Renmark Group sediments has marginal marine influences, indicating that deposition took place within a coastal floodplain environment. The middle, mainly un· sampled interval, contains non-marine channel sands representing a progradational phase during a regional regression. The upper part of the unit was deposited in a paralic, mud flat environment associated with a widespread Oligo·Miocene marine transgression.
INTRODUCTION
This study is a facies analysis of Renmark Group sediments intersected in BMR Woodlands No.1 borehole from the Murray Basin, New South Wales. Detailed lithological logs of Renmark Group sediments recovered from the borehole are presented, as well as a discussion of depositional environmcnts encountered in the interval 227-370 metres.
The Woodlands borehole is located in the Ana Branch 1:250 000 topographic sheet area at 33°17'14"S and 141°50'56"E at an elevation of 58.2 metres above sea level. The total depth of the borehole is 396 metres. Unfortunately basement rocks were not intersected, and wireline logs were only recorded from 0 - 340 metres.
Core recovery in the Renmark Group was poor due to the unconsolidated nature of the sediments, in particular the sand facies; consequently only 40% of the section was recovered. Much of the recovered material was broken or in a poorly preserved state. Geophysical wireline logs were invaluable in deciphering the nature of missing core.
GEOLOGICAL SETIING
The Murray Basin is an intracratonic basin containing thin, flat lying Cainozoic sediments which extend over an area of 320,000 km2 of southeast Australia (Fig. 1). The Cainozoic succession unconformably onlaps Proterozoic and Lower Palaeozoic basement blocks and Fold Belts to the northwest and west, and a Palaeozoic Fold Belt to the south and east. Locally underlying the Cainozoic sediments in the northwestern areas are a series of troughs which contain thick, block-faulted but relatively undcformed Devonian sediments. Erosional remnants of Upper Palaeozoic and Mesozoic platform cover sediments also occur in troughs and depressions beneath the Murray Basin (Fig. 2).
The Cainozoic stratigraphy of the basin and the approximate stratigraphic position of Woodlands No. 1 are depicted in (Fig. 3). Figure 4 outlines the biostratigraphic age, lithology and stratigraphy intersected in Woodlands 1. The Renmark Group is divided into the Olney Formation and Warina Sand in New South Wales and Victoria; equivalent to the Upper and Lower Renmark beds in South Australia (Brown & Stephenson, 1986). This report describes the Eocene to Oligocene Olney Formation and the lower part of the overlying Ettrick Formation / Geera Clay.
2
Fig. 1 Locality map
D Cainozoic Murray Basin
D Concealed Permian. Triassic, Cretaceous infra basins
~ Mid-Lower Devonian to Lower ~ ~a~~~;~~r~rt~ ?ra;~\~~eBasln, and
~ ? Upper Siluri~n to Mid-Lower ? Devonian Darling Basin. Melbourne
- Trough, and Gramplans area
1"<:::<>:1 Cambro -,Ordovician Scopes ". ..... Range High
O ? Cambrian volcano - magmatic arc ~ v intruded by Devonian granitoids
(Stavely Hlgh,Lake Victoria High. Lake Wintlow High)
The Cainozoic depositional history of the basin records three major marine transgressive events which occurred during the Late Eocene, Oligo-Miocene and Pliocene. With the exception of the carbonate-dominated marine units of the Oligo-Miocene, most of the sediment deposited during these events have a high siliciclastic component. Fluvial to fluvio-Iacustrine sedimentation dominates much of the basin in the north and east, with arcuate belts of transitional marginal marine sediments rimming the on and offlapping marine sediments to the southwest.
Woodlands No. 1 was sited over a concealed gravity feature, the Lake Wintlow High, to conduct hydrological sampling and to test the existence of shallow basement in the area. Intepretation of an aeromagnetic feature, predicted a basement depth of 200 metres below sea-level. Drilling indicated that the basement was well below 200 metres, in fact, in excess of 400 metres below sea-level. Structure contours produced for the base of the Renmark Group (Fig. 5, Campbell Brown, pers comm, 1988), have shown that the area beneath Woodlands 1 was a topographic low during the Early Tertiary.
Post orogenic platform cover
Lower - mid - Palaeozoic Lachlan Fold Belt (undifferentiated)
• Lower Palaeozoic
~ Kanmantoo Fold Belt
F:.:::-::I Proterozoic (AdelaideanJ to lower :::::::::: PalaeOZOIc Adelaide Fold Belt
lIi£1 Precambrian Willyama .,":,\1 Basement Block
Concealed aeromagnetic trend lines
Boundary of major tectontc elements
Boundary of minor tectonic elements
19/A/61
Fig. 2 Framework tectonic elements and underlying infrabasins (Brown & Stephenson, 1986)
3
TERTIARY STRATIGRAPHY OF MURRAY BASIN East
EPOCH
AGE Ma West
E.~~~i;~~~~~~~;~{~~~~~~~~~~lt~. Formation Tragowel Member~ / LWandelia Sandstone Mbr -(Wunghnu Groupl __ - Torrurnbarry Clay-~
PLIOCENE tale
Early !i
Late
10
MIOCENE Middle
-Fmnls Clay
iCadel1 I Marl
EROSION. NON-DEPOSITION ?
-J'rJJ'J'I~~~~ --L
,r:!.........':"""'" ---J....-~ Pota limestone
Morgan limestone
Early 20-
late
OLIGOCENE
Early
late
EOCENE Middle
50
Early 55
Late 60
PALEOCENE
Eall~ 65 ~ ~ ~ Conglomerate ~ Sand
I I ? L Kerang Sand Member LATE TERTIARY HIATUS ?
NON-DEPOSITION
EROSION OF PRE-TERTIARY
§CI8V El Lignite ~ Limestone ~ Marl
(Renmark Group)
~DOlom!te
19/A/160
Fig. 3 Cainozoic stratigraphy of the Mlm·ay Basin, alld approximate stratigraphic position of Woodlands 1 bore (Brown & Stephenson, 1986)
The extent of the Oligo-Miocene and Pliocene marine transgressions within the Murray Basin have previously been well defined, whereas the extent of the Late Eocene marine transgression is poorly known, and one of the purposes of this study is to ascertain the extent of marginal marine to marine inOuence during the Late Eocene. As Woodlands No.1 is located to the north of any previously known occurences of Late Eocene marine sediments in the basin it is ideally suited for this purpose.
LITHOFACIES
GENERAL DESCRIPTION
The Renmark Group sequence between 231 and 259 metres and 328 and 370 metres is composed of light to dark grey, unconsolidated to semiconsolidated, fine to coarse-grained, quartz sand and carbonaceous, laminated, clayey silt and fine sand and clay. The uppermost section of the sequence from 231 to 245 metres consists of finely laminated and intensively burrowed silt, clay and fine sand. The upper boundary of the Renmark Group in Woodlands 1 at 231 metres is taken from a 'log-pick' on the gamma and neutron logs. Unfortunately there was no core recovery for this interval. Above 229.5 metres, however, glauconitic and bioturbated clayey sands of the Geera ClaylEttrick Formation are present.
Figures 6,7 and 8 depict lithogies, biological properties and interpreted lithofacies of the sediments recovered, from the middle of the Geera ClaylEttrick Formation to the base of the Renmark Group. The unsampled interval between 258 and 328 metres is interpreted from geophysical logs as a thick channel sand sequence, possibly point bar deposits. Four lithofacies A,B,C, and D are differentiated on lithological, sedimentary structure and biological properties. Two of these facies have been further divided into subsets i.e. Bl, B2, B3 and Cl, C2, C3.
LITHOFACIES A: GLAUCONITIC SAND
Characteristics: Glauconitic, pelletal, bioturbated, medium- grained, clayey sand (Plate 1).
4
AGE
I.IJ z: I.IJ u 0
.... C-
I.IJ z: I.IJ U 0
~
I.IJ z: I.IJ U 0
"" .... 0
I.IJ :z: I.IJ u 0 I.IJ
ZONE
'" ::>
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:z:
WOODLANDS - 1
DEPTH LITHOLOGY
0
50
100
150
200
250
300
350
400
2 - - - --~"'--. .:....~---
6 '- :. -'. - '.-!-
'- ..:. - -- - -., -. - -' '--- - -56 -~ -." -- - .
. '-"!'
- .. "7"
13 0 I-z:-"-.~,,;. : .... .:z:._.-.'-. -i,
-- - - --
187 j::-J:=D::I~ 191 _ _ __ -- - -~ ~'" -
2 2 3 _. __ • :- ._ • - .• ..=- ~-
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"; ... ', . '.
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. ~-'.-,_ -0°
:-.• ,' • '..!',.
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. '.'-'
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. . . .
T. D. 396 metres
33 17'14" 141 50'56"
R.L. 58.2 m
STRATIGRAPHY
Woorinen Fm Blanchetown Clay
Parilla / Loxton Sands
Loxton Sand I Renmark Gp
Bookpurnong Beds I Geera Clay
Winnambool Fm Duddo Limestone
Winnambool Fm
Geera Clay I Ettrick Fm
RENMARK GROUP
• Not sampled
MURRAY
GROUP
Fig. 4 Woodlands 1 - stratigraphy
BURRA
'OOlo.m I
I"
0
t .. ""
-200
\ W ALE S
l \ \
T········I :' : .. ' :: .... ::
-400
5
Fig. 5 St/'llcture cOlltollrs all base of Renmad( Group, Mun'ay Basin, ill metres relative to sea-level (data provided by CM. Browll)
Description: Dark grey olive, poorly indurated to indurated, medium-grained, pelletal, clayey, quartz sand; fair to poorly sorted with muddy, carbonate-rich matrix; fecal pellets are replaced with glauconite and comprise approximately 20% of the facies; Abundant organic particles including small twigs, shell fragments and partially dissolved forams are present; Abundant reworked, rounded, dark grey mud intraclasts have rust-coloured, mottled, iron-rich rims.
Stratigraphic Position: Lithofacies A occurs between 227.5 to approximately 231 metres, above a finegrained, bioturated laminated facies, and below bioclastic carbonates of the Murray Group. This facies is part of the Geera Clay/Ettrick Formation, and produces an upward fining cycle on log profiles.
Depositional Environment: The presence of glauconite, fecal pellets, carbonate-rich matrix, and fossil debris suggest that these sediments were probably deposited in a range of marginal marine, interdistributary bay to lagoonal environments. The presence of sand within the unit suggests deposition in rclatively close proximity to a fluvial channel which may have been the source of the sands. The sands show considerable evidence of reworking, which suggests a sand bar or sand channel environment. The fecal pellets were probably deposited in situ and replaced with glauconite in a mildly reducing environment. Nearby intertidal-supratidal mudflats may have provided the intraclast 'mudballs' which were reworked to produce their rounded appearance.
6
220
250
300
350
370
GAMMA NEUTRON
'-.. ', . ::',: : :-.... : .. : .. ,-
- . ..' :.. .. '. ,', ,'::':.::,
,,' ...... , . ~ ; . . . '. ..
LITHOFACIES LITHOLOGY
A
CI
=0 CI
===D --B3
:==0
B:2.. =D =D B,- 0
==.e.')
Dark grey olive, medium grained quartz sand, glauconitic fecal pellets. pyritic and bioturbated with abundant mud intraclasts.
Medium to dark grey, finely laminated, sHty clay and fine sand, intensive burrowing, pyritic, mud intraclasts.
FIne to medium grained quartz sand, silty matrix. subangular to sub rounded grains, traces of ?ilmenite in minor, fine, Silty peat hor izons.
Light grey to grey white, cross-stratified, fine grained sands, with very thin, interlaminated siltstones and peat horizons; palaeosol and rootlets.
Poor recovery / unsampled interval
Fissile. laminated and cross-laminated, medium to dark brown grey, micaceous clayey Silt. with light-medium brown grey fine quartz sand; organic-rich, abundant plant fragments.
Carbonaceous, dark grey to block, clayey silt to silty clay, massive to faintly laminated.
Light grey, friable quartz sands, medium to very coarse grained. rare ct'c:>ss-bedding, lignitic fragments.
Light to dark grey, poorly sorced, coarse to fine sands, with silty lenses, and upward fining <:oarse sands and silts.
Fig, 6 Lithostratigraphic column of the Renmark Group in Woodlands 1
7
c3.3
0
22.0 . ^,
P . a .• Fi.sWar
P
U
a 1111 •Po.c0115
F; s 5
[
G
a
G
.....
I I asMI
I •P issP. tossP. co. ,.s
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li IIa a
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PcP e or DI ky
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I 1
a•
111we
gi4S
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I • • Biky?Fr VA cons
350P P. co.s
aII FI:
4 • IF: 5g; SC
370 9 I NI • . A COKG
CG-e. Asc,„„,ee yr t00%75TOA G
Fig. 7 Sedinzentaty Features of the Renmark Group
7 "J
i C i .:..:: c ~ ::J C5 \:) 0 0 -u <>.J w s:: :..,::. .~ i ~ "" '-J
N ·E d 4-.... C c: .3 c
~ -t-
'C 0') -3 ·e .~ .~ Vl
] >- c c:5 c.. 0 J::: ] ~ ·cs d ..9 --' <.1\ '- ~ Q) -.l :; c..n 0- Q.l a.. <U ~ Q.) <C J: > a Q III :1l .:::l :j -0- a 00\- (5 >- .4:: oil -a.. '"- ~ 0- u c.. c.. :;:r .c: (] <l.. 0 <f1 <:l
Q.) IlJ 0 &
<S Q) c.. <:2 t- O <3 CJ d. cSv f JVIc9 c.n ~ -I c..::J Cl a z
p • • • F"i.'>~
• EtuJ..,.
• f;~~ G f. coos p • • • F'·$~
I • - t= is~ -c. I • P. (.O~!. P. Co"S - VII'~~~ ri-e..
c. P. c.O;o!.
rf • • (t<\W I P • I\.~~y
300
P 1)1 k.'V c: • • F;6!> p
I I Blk.,
C I • ~i~s
• - r=i~ G •
I • • BII"y Mop u .... ~o,,!,
P - P. COI'I~
• I I I • 1=. !.~
~ F;~~ • • J::"i\S P • • • • P'Co.,!.
Core. Ae..c.o~er,# Fig. 7 Sedimentary Features of the Renmad, Group II" 'DO-J.
7S" (0 a'
8
CI w:: t: <Jl ..J U 0-R. A It A
220
• • • I I I I f ~ • • • • • • I I
• • • • • • • • • • • • - 1--250 •
•
-!-300
• • • • • •
• • • • • >
• • • - )50 • -
• • • • • - )
• ~ • • • - ) • • • ) • • • • 310 • • • > :
Fig. 8 Biological properties of the Renmark Group R. - AAN2
A - AbLll'\dGnt
9
LITHOFACIES BI: BIOTURBATED SAND AND SILT
Characteristics: Intensively bioturbated and pyritic, finely laminated, silty clay and fine-grained sand (Plate 1).
Description: Fissile, light grey to dark olive grey, finely laminated, silty clay, with intcrlaminated fine to very fine, silty quartz sand. Laminations range from parallel to lenticular and are 1-4 mm in thickness. The sediment is extensively burrowed with both horizontally and vertically orientated small ( < 1 mm) and large (> Imm) burrows, which are filled with silt, fine sand or pyritic material. Very small mud flakes arc common throughout the sequence, as well as abraded, finely divided plant fragments, that are somctimes pyritised. Much of the sediment is carbonaceous and occasionally has a sulphurous odour.
Stratigraphic Position: Lithofacies Bl is approximately 7 metres thick and occurs between 231 and 244 metres, below the Geera Clay/Ettrick Formation. It is interpreted as the stratigraphic top of the Renmark Group, and produces a linear log profile on geophysical logs.
Depositional Environment: The finely laminated nature of the sediment, the occurance o[ mud flakes and intensive burrowing, by both large and small organisms, indicate that this unit was probably deposited in a marginal-marine mudflat environment. Oxidation conditions changed during deposition of these sediments, [rom reducing to mildly oxidising, attested by the varying colour, odour and pyritic content of the material. The finer grained sediment accumulated under low energy conditions.
LITHOFACIES B2: SAND AND SILT
Characteristics: Monotonous, fissile, finely laminated, fine-grained sand and clayey silt (Plate 2).
Description: WeB sorted, medium to dark brown grey, laminated, micaceous, clayey silt, with interlaminated light to medium grey, quartz-rich, silty sand. The sands contain sub-angular to sub-rounded grains with very minor altered feldspar. They occur as lenticular, cross-laminated and low-angle ripplelaminated horizons, and form approximately 30% of the lithofacies.
Organic material is common and occurs as finely divided to well preserved, earbonised rootlets, twigs and leaves. The finer grained sediment occurs as very thin (1-5 mm), parallel to wavy laminated layers. Burrows arc extremely rare and very low percentages of marginal marine dinoflagellates arc present throughout the sequence. Pyritic nodules are present but are not abundant.
Stratigraphic Position: Lithofacies B2 occurs in two intervals, each approximately 10 metre thick, from 331.2 to 344, and 357 to 369.6 metres. These units are separated by a coarse grained sand facies.
Depositional Environment: The relatively thick, carbonaceous and laminated nature of this facies suggests deposition in a well vegetated floodbasin environment. Poorly-drained to well-drained swamps and lacustrine environments characterise floodplains. The coarser grained fraction of the sedimcnt represents overbank flooding events, and the finer material is a result of settling of suspended sediment. Reworking of sediment is common on floodplains and consequently biogenic structures are often not preserved.
Various depositional environments are represented by Lithofacies B2. The light grey scdiments, with a high silt to organic debris ratio, were probably deposited in well-drained swamps. Conversely, the olive grey-black organic-rich silts and mudstones, with relatively common pyrite and siderite nodules, represent deposition in poorly-drained swamps and lacustrine environments. The presence of dinoflagellates suggests that these sequences were deposited in distal reaches of a river system close to marine or marginal-marine environments.
LITHOFACIES B3: COARSE SAND AND SILT
Characteristics: Poorly-preserved, carbonaceous, laminated, coarse-grained sand with mlJ10r interlaminated mud (Plate 2).
Description: Medium dark brown grey, poorly sorted and bedded, medium to coarse-grained sand with minor carbonaceous mud. Mud intraclasts, lignitic particles and plant remains are commmon. A crude fining-upwards sequence is present in one section but poor preservation, due to the unconsolidated nature of the sand, sedimentary structures are absent. Deposits are thin, with an average thickness of approximately 0.5 metres.
Stratigraphic Position: Lithofacies B3 occurs at 3 intervals within the Renmark Group, at 237.2 - 237.8, 330.5 - 331.2 and 369.6 - 370.1 metres (base of recovery of Renmark Group sediments). Lithofacies B3 occurs within Lithofacies Bl (?mudflat) and B2 (f1oodbasin).
Depositional Environment: Lithofacies B3 consists of crevasse splay deposits which contain a variety of scdiment typcs, ranging from coarse sands to silty clays and lignitic particles, reflecting the varied dcposi-
10
PLATE 1
LITHOFACIES A - GLAUCONITIC SAND
a. Indurated clayey, dark grey olive, fine to medium grained glauconitic sand; bioturbated, mottled, pelletal with mud intraclasts; sand filled 1 em wide burrow at top, centre of core. Core 27, 228.3 metres.
b. Photomicrograph of Core 27, (Plate la); glauconitic fecal pellets in bioturbated, poorly sorted clayey sand; Crossed polars, field of view 6 mm high.
LITHOFACIES BI - BIOTURBATED SAND AND SILT
c. Burrows in laminated, carbonaceous, medium to dark olive grey silty clay and fine sand; burrows filled with silt to fine sand with pyritic and/or glauconitic matrix; Core 30, 236.4 metres.
d. Bioturbated light grey, laminated silty clay with poorly consolidated fine sand laminae; Core 30, 238.0 metres.
e. Horizontal burrows in laminated light to medium olive grey silty clay with fine to medium grained sands; Core 30, 237.2 metres.
f. Photomicrograph of core 30,(Plate Ie); Silt to fine grained sand filled burrows in upward fining laminated silty clay; black fragments are organic particle; Crossed polars, field of view 10 mm high.
(Scale bar in 1 centimetre increments)
PLATE 1 11
a
PLATE 2
LITHOFACIES B2 - FINE SAND AND SILT
a. Micaceous medium brown grey silts with cross laminated and ripple laminated,poorly consolidated, fine sand laminae, 0.1 - 2 mm thick; Core 49, 359 metres.
b. Photomicrograph of Core 49 (Plate 2a); well sorted silts with silt sized abradedplant fragments; sand laminae removed during slide preparation; field of view10 mm high.
c. Small twigs and lignitic fragments in light to medium brown grey silts; Core 42,341.8 metres.
d. Wavy to parallel finely laminated medium brown grey silts with light tomedium grey, fine grained sands; Core 49, 358 metres.
e. Well preserved unidentified leaf; Core 49, 359 metres.
LITHOFACIES B3 - COARSE SAND AND SILT
f. Large (1 cm) pyrite nodule distorting laminated silts with fine to mediumgrained sands; curved appearance of core partly due to disruption of structureduring drilling.
(Bar scale in centimetres)
12
II1^1111111111111*R9 0 0 0 2 0 3*
PLATE 2^ 13
C
e^ -I"
PLATE 3
LITHOFACIES Cl - SAND DOMINANT.
a. Very friable, light grey, fine to medium grained quartz sand; dark disconnectedhorizon is silty lignite; Core 33, 247.5 metres.
b. Photomicrograph of Core 33 (Plate 3a); Sub-angular bimodal quartz grains withwell orientated angular quartz shards in moderately well sorted sand; Crosspolars, field of view 10 mm high.
LITHOFACIES C2.
c. Photomicrograph of Core 36 (Plate 3e); well sorted, laminated fine grained siltysand; peaty fragments and silts form distinct laminae; Plane polarised light,field of view 1 Omm high.
d. Well preserved plant root in leached, bioturbated, silty sand (palaeosol); fieldof view 3cm wide; Core 36, 255.2 metres.
e. Light grey, fine grained silty quartz sand; cross laminated with approximately 20dip; Core 36, 256 metres.
L1THOFACIES C3.
f. Photomicrograph of Core 47 (Plate 3g); sub-angular to sub- rounded, poorlysorted quartz grains in coarse grained sand. Cross polars, field of view 10 mmhigh.
g. Very friable coarse grained, light grey quartz sand; black fragments are lignite;dark patches are lenticular fine sand/silt beds; note cross stratification of verycoarse quartz grains at top of the core; Core 47, 353.1 metres.
(Bar scale in centimetres)
14
1111410110
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PLATE 4
LITHOFACIES D - SILT DOMINANT.
a. Photomicrograph of Core 38 (Plate 4b); structureless, faintly laminated clayeysilt with rare fine quartz grains; quartz rich silt with 5 -10 % weatheredfeldspar and mica; Cross polars, field of view 6mm high.
b. Dark brown grey, parallel finely laminated, organic rich clayey silt; Core 38,330.2 metres.
c. Dark grey, finely laminated, organic rich, micaceous clayey silt; the thin crack inthe centre of the core is due to shrinkage during core preparation; Core 52,366.7 metres.
d. Black faintly laminated carbonaceous silty clay; light 'stringers' are organic richsilts possibly due to dewatering or differential compaction; Core 51, 365.3metres.
(Bar scale in centimetres)
16
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a
b
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PLATE 5
SEM PHOTOGRAPHS OF SAND DOMINANT FACES.
a. Montmorillonite clay on pore-linings surrounding detritial quartz grains; notelarge pore spaces; small 'dusty' grains are possibly kaolinite; Core 33, 247.55metres; magnification X 220.
b. Enhanced view of authigenic montmorillonite from Plate 5a;magnification X 4400.
c. Montmorillonite from Core 47, 353.1 metres; magnification X 2200.
d. Probable kaolinite 'booklets' distributed around quartz grains from Core 47(Plate 5c); magnification X 2200.
(Photographs provided by Julie Kamprad)
18
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20
tional conditions typical of crevasse environments. Crevasse splay deposits result from major flood eventsthat cause breaching of natural levees, and produce sheet flows with high sedimentation rates. Plate 2f il-lustrates a crevasse splay deposit which possibly formed at the distal end of a sheet splay. Thestratigraphic position of this lithofacies within floodbasin and fine grained paralic sequences, is typical ofcrevasse splays.
LITHOFACIES Cl: SAND DOMINANTCharacteristics: Unconsolidated to friable fine to medium- grained sand with minor peaty silt horizons(Plate 3).Description: Light to medium grey, fine to medium-grained quartz sand, with minor muddy matrix. Thesands are mainly unconsolidated, porous, moderatedly well sorted and contain sub-angular to sub-roundedquartz grains. Rock fragments, e.g. acid volcanics and chert, mica, altered feldspar and traces of ?ilmeniteconstitute less than 5% of the sands. Preservation of sedimentary structures is poor, although crude planelamination was noted. Thin, minor peaty silt layers are also present. Iron rich mottles are also present,but are probably due to iron precipitation from pore waters present in the bagged samples. Abundantfresh water algae was recovered from the base of the unit, with a notable absence of marginal-marinealgae.Stratigraphic Position: Lithofacies Cl occurs between 245.5 to 251.1 metres, beneath the bioturbated finesand and silt facies, and overlies Facies C2. This facies produces a serrated bell shaped log profile ongamma and neutron logs.Depositional Environment: Due to the absence of preserved sedimentary structures interpretation of thisunit is somewhat tenuous. However, the sandy unconsolidated nature of the sediment, lack of marine fos-sils, shape of the log profile and presence of minor peaty silt, suggest a channel fill environment, possibly?levee deposits.
LITHOFACIES C2: SAND DOMINANTCharacteristics: Poorly consolidated, cross laminated, leached fine to medium-grained sand (Plate 3).Description: Light grey to grey white, friable, well sorted and cross laminated, silty quartz sand. The sandgenerally consits of fine-grained, sub-angular particles containing between 5-10% kaolin and plant remains.Laminae are defined by silt or silty peat horizons and vary from 1-4 mm in thickness, with a dip of ap-proximately 200 . Overlying the cross laminated sands are leached, ?churned, silty sands with abundantwell preserved rootlets.Stratigraphic Position: Lithofacies C2 is present between 255 - 256.3 metres, and underlies Facies Cl. Itis separated from Cl by a 20 cm thick organic rich mudstone.Depositional Environment: The presence of cross laminated silty sand, overlain by a leached, root biotur-bated sediment, suggests a well preserved natural levee deposit. The leached sediment containing rootletsrepresents a palaeosol. This facies may belong to overlying Facies Cl, however, as it is so well preserved,a separate facies is warranted.
LITHOFACIES C3: SAND DOMINANTCharacteristics: Poorly consolidated, friable, coarse sand, fining upwards to laminated sand and silt (Plate3).Description: Light to medium grey, very coarse to fine-grained, poorly sorted, quartz sand containingminor rock fragments. Cross stratification was noted, although most of the sample was structureless. Thefacies fines upwards into a medium to dark grey, organic rich, silty mud with interlaminated light grey,coarse grained sand. Mud clasts are relatively common in the middle of the unit, and lignitic fragmentsand pyrite nodules are present throughout the sequence.Stratigraphic Position: Lithofacies C3 is present from 346.3 to 356.5 metres, and overlies Facies B2(floodplain deposits), with what appears to be an abrupt lower boundary. Core recovery was poor due tothe unconsolidated nature of the sediment.Depositional Environment: The upward fining character of Lithofacies C3 and abrupt lower boundary ofthe sandy sequence suggest a channel fill depositional environment, possibly point bar deposits. The thick-ness of the unit, presence of cross stratification, coarse-grained nature of the sands and presence of mudclasts, support this interpretation.
lj 01,11,11!
21
FACIES D: SILT DOMINANTCharacteristics: Faintly laminated, carbonaceous clayey silt to silty clay (Plate 4).Description: Dark brown grey to black, carbonaceous faintly laminated silt and clay. Delicate laminae aregenerally parallel and are readily distinguishable within the fine-grained deposits. The clayey silts arepredominantly quartz rich, highly organic and occasionally micaceous. Between 344.4 - 344.8 metres, blackcarbonaceous, silty clay forms small-scale (about 10 cm) upwards-fining cycles, with increasing carbon con-tent.Stratigraphic Position: Lithofacies D occurs mainly within the floodplain Fades B2 in approximately 20cm intervals from 365 to 369.5 metres, and at the base of B2 between 344.1 - 344.8 metres. It is alsopresent in the middle of Lithofacies Cl at 252 metres and above the interpreted crevasse splay deposit at328.9 metres.Depositional Environment: The highly carbonaceous and faint, parallel laminated nature of the lithofacicssuggests deposition in very quiet water environments, probably lake or poorly drained swamp deposits.
DIAGENESIS
Clay Analyses: A cursory analysis of clay minerals within the sequence was undertaken. Samples wereanalysed from the fine grained Facies B1 and D, and from the sand Facies Cl and C3. The analysis weredone by Julie Kamprad, BMR. The fine grained units sampled contain a mixture of smectite and kaolinclay.
The coarser grained sand facies also contain smectite and kaolin as well as traces of mixed layerclays. SEM photographs of sands (Plate 5), shows that the authigenic smectite forms a thin pore-liningaround detrital quartz grains. The kaolin appears to form scattered `flakes' and small 'booklets' on thequartz grains. Substantial quartz overgrowths on the quartz grains were not evident on the photographs.The authigenic smectite and kaolinite are a result of precipitation from K, Na, Ca and Mg richgroundwaters flowing through the sands.Other Minerals: Glauconite forms in mildly reducing marine environments. The glauconite in Fades Aoccurs mainly as replaced fecal pellets but does occur as discrete grains. Pyrite is ubiquitous in Facies Aand B1, and does occur to a lesser degree in Facies B2. It replaces organic material, e.g. rootlets andtwigs, as well as certain types of burrows, and also occurs as nodules. The iron sulphide was probablydeposited from sulphate rich water under suitable reducing environments, produced by organic material,during initial sediment deposition and remobilised during diagenesis.
The poor presevation and recovery of Renmark Group sediments reflects the generally low level ofdiagenesis effecting the sequence. The diagenic effects of the sediments varies depending on the type oflithofacies. Sand facies show negligible diagenesis, and consequently high porosity, except for minorcompaction and growth of authigenic clays. In contrast, the laminated fine elastics have been compactedand de-watered to produce fissile, partially consolidated muds. The rank of carbonaceous material alsovaries between lithofacies, from a peat to a low grade lignite in de-watered muds. The interlaminated finesands and silts are generally unconsolidated.
DISCUSSIONPublished information on the regional depositional setting of the Renmark Group sediments, in the
northern part of the Murray Basin, suggest deposition by a southward flowing fluvio-lacustrine system.Based on the lithological, sedimentological and biological properties of the sediments analysed inWoodlands No. 1, a genetic relationship between facies can be proposed. The interpreted depositionalenvironments encountered, appear to be related to a regional transgressive and regressive cycle. The baseof the sampled sequence was deposited during the Late Eocene in a broad, flat-lying floodbasin/coastalplain (Fig. 9). These sediments are probably a lateral equivalent of marls of the marine Buccleuch bedsrecognised to the southwest. The presence of carbonaceous floodplain Facies B2, B3 and D (Table 1),with the associated channel deposits C3, as well as the presence of marginal marine algae implies that the`palaeo' water table was sufficiently high to preserve the carbonaceous content.
Overlying these sediments is a mainly unsampled interval, probably representing fluvial sand deposits,which appear to contain only fresh water algae (Facies Cl and C2). A widespread Oligocene erosionaland/or non-depositional hiatus has been recognised within the basin (Brown & Stephenson, 1986), whichhas been related to a regional marine regression. This hiatus caused a lowering of base level, which
22
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RENMARK GROUP DEPOSITIONAL ENVIRONMENTS
TOP RENMARK - ETTRICK FM/GEERA CLAY
DEPOSITIONAL ENVIRONMENTS
Fig. 9 Schematic reconstruction of depositional environments of Renmark Group in Woodlands-l bore.
23
FACIES LITHOLOGY^ DEPOSITIONAL ENVIRONMENT
A ^ Glauconitic sand, mud intraclasts ^ Marginal marine, interdistributary bay to lagoon
B1^Laminated fine sand & silty clay ^ Marginal marine mudflatB2^Laminated micaceous clayey silt ^ Floodplain, lower reaches of river system^ & fine sand
B3^Coarse to medium sand, minor mud^
Crevasse splayCl^Fine to medium sand, minor mud, peat
^Meandering river channel
C2^Cross stratified fine to medium sand .^Meandering river channel - levee
C3^Coarse sand & minor laminated sand .^Meandering river channel - point bar^ Laminated silty clay ^ Open to marginal lacustrine to swamp
Table I Lithofacies and interpreted depositional environments
caused an increase in erosion, and could reasonably be interpreted to lie within the unsampled non-marineinterval.
This regressive sequence is overlain by a marginal marine, bioturbated, laminated sequence (B1) anda glauconitic clayey sand (Lithofacies A), which represent a well documented Oligo-Miocene marinetransgression. The structure contour map of the base of the Renmark Group indicates that the area in thevicinity of Woodlands No. 1 was probably a broad valley draining a large hinterland to the north. This issupported by the diversity of floras recovered from the sediment encountered in Woodlands No.1, incomparison to floras recovered from equivalent intervals sampled elsewhere within the basin (McPhail, inpress).
This relatively flat, low-lying region, was readily affected by regional sea level fluctuations throughoutthe Cainozoic, and is part of a major SW-NE orientated depositional axis in the northwest of the basin.
ACKNOWLEDGEMENTS
The writer thanks Phil O'Brien and Bruce Radke for helpful discussions related to the faciesintersected in the borehole. Campbell Brown and Ray Evans provided useful discussions concerning thesediments within the Renmark Group. Appreciation is also due to Ken Heighway, Arthur Wilson, JoeStaunton and Eddie Resiak for logistical support. Julie Kamprad kindly provided the clay analysis andelectron photograghs and Jennie Totterdell helped with typing. The text was edited by Campbell Brown.
REFERENCES
BROWN, C.M. & STEPHENSON, A.E. 1986 — Murray Basin, southeastern Australia: subsurfacestratigraphic database. Bureau of Mineral Resources, Geology & Geophysics, Report 262.
COLEMAN, J.M. 1966 - Ecological changes in a massive fresh -water clay sequence. Transactions — GulfCoast Association of Geological Societies, XVI, 159- 174.
COLEMAN, J.M. & GAGLIANO, S.M. 1965 — Sedimentary structures: Mississippi River deltaic plain. InMIDDLETON G.V. — Primary sedimentary structures and their hydrodynamic interpretation. Society ofEconomic Palaeontologists and Mineralogists, Special Publication 12, 133 -148.
EKDALE, A.A., BROMLEY, R.G. & PEMBERTON, S.G. 1984 — Ichnology, The use of trace fossils insedimentology and stratigraphy. Society of Economic Palaeontologists and Mineralogists, Short Course 15.
ETHRIDGE, F.G, JACKSON, T.J. & YOUNGBERG, A.D. 1981 — Floodbasin sequence of a fine-grainedmeanderbelt subsystem: The coal- bearing Lower Wasatch and Upper Fort Union Formations SouthernPowder River Basin. In ETHRIDGE, F.G. & FLORES, R.M. — Society of Economic Palaeontologistsand Mineralogists, Special Publication 31, 191-209.
GALLOWAY, W.E. 1981 — Depositional architecture of Cenozoic Gulf coastal plain fluvial systems. In -
ETHERIDGE, F.G. & FLORES, R.M. — Society of Economic Palaeontologists & Mineralogists, SpecialPublication 31, 127- 155.
HARRIS, W.K. 1980 — Eocene eustasy and the deposition of lignites in South Australia. Abstracts In WIL-FORD, G.E. The Cainozoic evolution of continental southeastern Australia. Bureau of Mineral Resources,Geology & Geophysics, Record 1980/67
MACPHAIL, M.K. in press — Palynological analysis: BMR Woodlands - 1 borehole, Murray Basin. Bureauof Mineral Resources, Geology & Geophysics, Record
24
MIALL, A.D. 1982 - Analysis of fluvial depositional systems. American Association of Petroleum Geologists, Education Course Note Series 20.
RADKE, B.M. in press - Sedimentology of Renmark Group sediments intersected in the Murray Basin. Bureau of Mineral Resources, Geology & Geophysics, Record.
REINECK, H.E. & WUNDERLICH, F. 1968 - Classification and origin of flaser and lenticular bedding. Sedimentology, 11,99-104.
WENTWORTH, c.K. 1922 - A scale of grade and class terms for clastic sediments. loumal of Geology, 30, 377-392.
WING, S.L. 1984 - Relation of palaeovegetation to geometry and cyclicity of some fluvial carbonaceous deposits. loumal of SedimentalY Petrology, 54 (1), 52-66.
25
APPENDIX 1
DETAILED LITHOLOGIC LOG OF WOODLANDS NO.1 BOREHOLE - EXPLANATION AND LEGEND
SAMPLE
LITHOLOGY
SORTING
DESCRIPTIONS
CORE APPEARANCE
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F T P C
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photograph thin section pollen analysis clay analysis
granule - very coarse sand (>1 rom)
coarse sand (0.5-1.0 rom)
medium sand (0.25-0.5 rom)
fine - very fine sand (0.06-0.25 rom)
silt (0.008-0.06 rom)
clay «0.008 rom)
carbonate
good fair poor
pyrite grained organic minor laminated subangular subrounded
ave average f fine vf very fine
friab fiss indur cons uncons blky conch crumb
dk med It gy bl gn 01 wh
friable fissile indurated consolidated (p - poorly) unconsolidated blocky conchoidal crumbly
dark medium light grey black green olive white
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APPENDIX 2
X RAY LABORATORY REPORT BMR WOODLANDS NO 1 (ANNA BRANCH 3),MURRAY BASIN
The following samples from the Olney Formation in the Murray Basin were presented to the X RayDefraction Laboratory for identification of the clay minerals. The samples were analysed under naturalconditions, treated with ethylene glyeol and analaysed again to give a treated and initial clay mineralidentifications.
A -5 u separation of the 247.55 metres and 353.00 metres sand samples, by defloculation and the useof a centrifuge instrument produced a good enhancement of the clays. The montmorillonitc gave a verydistinct pattern, and scanning electron microscope photographs were taken of kaolinite andmontmorillonite from natural core samples.
XRD LABORATORY RESULTS235.9 m (Fine-grained clay)
Dark fragments — pyriteWhole sample — quatrz minor, possible feldspar traceClays — montmorillonite major, kaolinite minor, mica trace
238.35 m (Fine-grained clay)Whole sample — quartz traceClays — kaolinite minor, montmorillonite minor, mica trace
247.55 m (Fine to medium-grained sand)Whole sample — quartz major, feldspar minorClays — kaolinite trace, montmorillonite trace,mica mixed-layer trace-5 sample kaolinite major, montmorillonite major, mica mixed-layer trace
328 m (Fine-grained silts,clays)Whole sample — quartz majorClays — kaolinite minor, mica trace
353 m (Coarse sand)Whole sample — quartz major, feldspar majorClays — possible montmorillonite trace-5 sample — montmorillonite major, kaolinite major
Julienne Kamprad
35
36