^ 7 H ft iò JJt/ j 9 o y THE GEOLOGY OF THE GREAT BARRIER BEEFS
IN PELATION TO OIL POTENTIAL
Dopothy Hiig, F>A.A.
f# The High Islands and Headlanls between Port Douglas and Sandy Cape •. •. p. 63
with list of references, p* 65
and annotated list •• p. 67
go Borings through Cays on Michaelmas Cay and Heron I. •• •• p. 83
(See also Appendix A)
This is followed by sections dealing with
related knowledge and theory that might help in
deducing what lies under the continental shelf
in areas covered by the Authorities to Prospect
of the Australian Mining and Smelting Co. (pages 85-120)
the titles to the sections and subsections being as
follows Î
B. The Geology (or Geomorphology) of areas adjacent to the Continental Shelf of Queensland and Papua •• p* 85
III. The Geology of Eastern New Guinea •• •• p* 86
with list of references .• p. 91
and Appendix I. Late Tertiary strat- igraphical sequence in Oriomo R. Area from W.M.Gray, A.P.O.,Vol.II .. p. 92 and Appendix II, Published infor mation on Bores drilled for Oil in Papua •• p. 93 .
IV. The Geology of Cape York Peninsula . • . • p* 94
with list of references •• p. 105
V. The Geology of the Queensland Coast South of Princess Charlotte Bay •• •• p« IO6
with Handbook to the Geology of Queensland (Appendix B) .. p.
VI. The Geomorphology of the Queensland Coast and Structural Hypotheses on the Continental Shelf developed from it •. •. p. 107
with list of references • • p. 112 VII* Major Structural Units of Queensland in relation to the Basement expected under the Queensland Continental Shelf . • • • p. 113
VIII, The Coral Sea .. .• p. 118
with list of references •• p, 120
Finally, the oil potential of the reef-bearing
parts of the Queensland-Papuan shelf is discuosed,
with recommendations for exploratory borings.
Tho titles to sections and subsections are :
C, Recommendations for Exploratory Work , • p. 121
IX, Tho Oil Potential of the Queensland-Papuan Continental Shelf between 143° E. the Great 3arrier Reef, and the Meridians of Bramble Cay and 11° S, (The Yorke Is, Platform) with recommendation for an exploratory boring ., •• ,, p, 123
X, The Oil Potential- of the Queensland-Papuan Continental Shelf between C, York (approx, 11° S,)and C. Melville (approx, 14° S.) with recommendation for exploratory boring ». », •• p. 127
XI, The Oil Potential of the Queensland Continental Shelf between C. Melville (14° So) and Hinchinbrook I, with recommendation for exploratory boring. •* p» 131
XII* The Oil Potential of the Queensland Cont inental Shelf between Hinchinbrook I. (18° S,) and Ft, Clinton (22° 20* S.) p, 133
XIII, Conclusion •• .• p, 136
Appendix G 0 Queensland State Geological Map, 1953
Australia Pilots, Vols. Ill and IV,
irts, a n n o t a t e d . 2 7 6 4 2763, 345, 346, A u s 0 1Ó4, Aus. 16 1 ç 347, 34Ö, 234-9, 2350, --WV ryr\ r\ ^ *-7¿4r¡P 2923. y A* o 2921, 2920, 2354, Â U S g 101, A u s e IO 2 ' Aus. 1C3, 2321. 1
A. THE KNŒJN GEOLOGY OF THE QUEENSLAND-»PAPUAN CONTINENTAL SHELF.
The Queensland continental shelf is continuous in the Gulf
of Papua with that of Papua, thus suggesting the two states are
part of the one continental mass. It will be considered in two
regions; 1. from Papua to the vicinity of Cape York, arid
11. that from Cape York to Sandy Cape.
A .l. THE SHELF IN THE GULF OF PAPUA AND THE TORRES ST. AREA.
In reading this section, use Charts 2764, Aus. 101, 102, 103.
The shelf is relatively wide at the Torres St. The outer
B a rrier Reefs stand somewhat westwards from the 100 fathom lin e ,
which from 11° S. trends N.N.E., while the line of the outer
Barrier Reefs trends northward along 144°. The maximum continental
slope would appear to begin at about the 100 fathom line, though
soundings are too sparse for accurate knowledge. The hundred
fathom line turns sharply E.S.E. when quite near the east shore
of the Gulf of Papua to form a narrow shelf that is in strong
contrast with the wide shelf on the western side of the Gulf.
There are four natural regions on this shelf. In one of
them, the delta region north of Anchor and Bramble Cays, the young
sediment on the shelf has been contributed from the rivers pouring
into the Gulf; some of the islands are of recent alluvium from
these rivers ; others, like Badu and Bristow are considered to
be formed from the updoming along E. - W. axes of Miocene-
Plioeene marine shelf deposits. (See p,87). This is out of the
Company’s authorityc The other regions will be described in
more d e t a il 2
GEOLOGY AND DISTRIBUTION OF THE CORAL REEFS IN THE GULF
OF PAPUA END TEE HEAD OF THE CORAL SEA TO 11° S.
Refer to Charts 2764? 2321, Aus. 101, 102, 103*
The reefs of the Gulf include great detached reefs outside the main barrier, barrier reefs, fringing reefs and inner
(platform or patch) reefs. Larger or smaller cays are developed on many and are apparently always of calcareous sand. I have no records of any shingle cays or ramparts such as are found on many of the Queensland inner reefs and island reefs J this may be due in part to difference in the strength of winds, and in part to the distribution of Queensland cyclones, none apparently strikin g North of about 12° or 11° south.
As Juices (1886) and many others have since observed, growth of coral reefs on the west side of the gulf of Papua and north of Bramble Cay is inhibited by the amount of mud poured out by the Fly and the other rivers of the Delta,
Also, south of this influence, there is a marked difference in the number of reefs developed on the west and east sides of the Coral Sea. On the western side, reefs are numerous from Torres Strait right across eastwards to the
144-th meridian, and, north of 11° S, to 144° 30! E. in 10° S. latitude. On the eastern side, reefs are developed only very close to the Papuan shoreline,
This striking difference may well reflect a difference 3
in sta b ility between the two areas. Eastern Papua is known to have been very mobile in the Palaeogene, and strongly
folded in the Miocene; whereas western Papua and Cape York
Peninsula are not known to have suffered any strong folding
since Palaeozoic times.
We are concerned only with the reefs of the western region. Here reefs growing from three different and quite
distinct platform-like areas can be distinguished.
West of the lin e running S.S.W. from the islands of
Badu and Bristow (where Miocene and Pliocene marine shelf
sediments are exposed) through Warrior, Dungeness, Long and
Three Sisters Reefs, to the eastern edge of the northern
part o f Cape York Peninsula, the reefs rise from depths no
greater than 10 fathoms, and many of them are reefs fringing
granitic islands.
East of the Warrior Line of Reefs, there lie s at about
the l^ t h meridian, the northern edge of the Great Barrier
Reefs, from East Cay through the Murray Islands and down to
Raine I. On their western side these Barrier reefs rise from
no more than 30 fathoms, while on their eastern side they may
rise from 80 fathoms or more. The flo o r o f the sea between
the Outer Barrier and the Warrior line rises from 30 fathoms
on the east, irregularly to 10 fathoms on the west. 4
Thus the platform West o f the Warrior line which we might
call the Torres Platform slopes very gently eastwardj that between the Warrior Line and the Great Barrier which we might
call the Yorke Platform, slopes a little more steeply. But the floor of each platform is irregular. Channels and banks
from which patch or platform reefs arise running either E - W,
or E.N.E. - W.S.W. are very numerous in the Yorke Platform, but
are largely unsurveyed or unexamined. Their orientation suggests that they may have originated on sedimentary trains given an E-W,
or E.N.E. - W.S.W. orientation by the currents generated by the
S.E. trades accommodating themselves to the shape o f New Guinea before being directed through the Torres Straits. But since very shallow E. - W. undulations have been detected in the Miocene-
Pliocene of the Oriomo sh elf region (Gray, 1928) these elongated reefs and reef trains may be based on small structural highs.
East of the Great Barrier, a third platform region of average depth 80 fathoms, diverges from the Outer Barrier at about 11° S. and trends N.E. towards the Lakekamu R. mouth. On
its east the Coral Sea falls very rapidly with its greatest change of slope for this western region. From the eastern part o f this eastern platform which we might c a ll the Portlock Plat form rise Boot and Portlock Reefs. This eastern edge forms the
100 fathom boundary o f the continental-shelf of Queensland-Papua.
The relationships of these three platforms each with a line
of reefs at its eastern edge, would seem, from géomorphologieal
considerations, to be :- 5
(a) The Warrior Lino, continuing as it doos along the line of
the E, shore of Cape York Peninsula, may represent subsequent
upgrowth of reefs begun as reefs fringing a continuation
of that shore which was drowned by faulting or warping.
(b) The Great Barrier Line is clearly the continuation of the
Queensland Great Barrier Reef, and must share at least the
latest geological history of that feature.
(c) The Boot Line is a feature without parallel in the northern
part of the Queensland continental shelf, and therefore in
dicates some geological incident which affected the region
north of 11° S. but not the region south of 11° S. It may be
that it represents an earlier continuation of the Great Barrier,
faulted or warped downwards by a deepening of the head of the
Coral Sea. Such a warping could well be related to the
olivine basaltic vulcanicity of the Murray Is, near the eastern
edge of the Yorke Platform. This type of vulcanicity is
characteristic of cratonic regions.
We are however without evidence other than geomorphological, of the dating of these assumed depressive movements in the Coral Sea
Basin. The only evidence we have is that the east coast of the north end of C, York Peninsula, which is on the southerly con tinuation of the Warrior Line, ‘looks young1 because of the general absence of cliffing. However this ‘youth1 may have been preserved for a very long time by the Barrier Reefs preventing heavy surf attacking the coast line.
The various cays and reefs mentioned in literature are listed, with references, in the Section “Calcareous Sand Cays and Shingle
Ridges on Reefs between Bramble Cay and Sandy Cape“ (pp. 30)• 6
B. THE HIGH ISLANDS OF THE TORRES STRAITS.
All who have considered these islands, which lie west of
142° 4 8 ‘ E. and (except for Booby I.) east of 142°, regard them as the tops of the submerged Peninsula ranges of meridional trend continued northwards into the New Guinea coastal plains,
(Jukes, 1847; Rattray, 1869; Haddon, Solías & Cole, 1894;
Maitland, 1892; Jack (in Jack & Etheridge 1892) and 1922; Morton,
1924; Richards & Hedley, 1925; Gray, 1928; Fairbridge, 1950;
Glaessner, 1950; Whitehouse, 1955; Jones & Jones, 1956),
Two igneous rock types, some schists and quartzites, and a little horizontal sandstone are known in them, similar in all cases to those of the Peninsula,
Granites are regarded by Morton (1924) as similar in type to those intruding the ? pre-Cambrian gneisses and schists of the
Peninsula, and unconformably overlain by the ? L, - Carboniferous
Pascoe R, Beds, The porphyries, which are quartz felspar por phyries, in part intrusive, in part extrusive and in part pyro clastic, are regarded by Morton (1924) as similar in all respects to those intruding the ? Lower Carboniferous Pascoe R. Beds and unconformably overlain by Mesozoic sandstones. The gneisses, schists and quartzites are like those of Somerset and Cape York,
The horizontal sandstone is ferruginous and siliceous and lateritized like the ? Aptian ^lythesdale’ of the Peninsula, with which it is correlated. The geology of the islands is thus very simple and I see no reason to doubt any of these correlations. 7,
The ferruginous, siliceous sandstones are known no further to the North than the Adolphus islands, and no further to thewest than Red Wallis Island*
The height of the islands is nowhere very great, 1,000 ft. being exceeded only on Banks Island, where the highest point is 1,310 ft.
Richards & Hedley (1925) considered that the islands of the southern part of Torres Straits were separated from one another and bounded by a fracture pattern along N.W. - S.Ë. and N.E. -
S*W. lines. This view was based on geomorphology only, no displacements of rocks being observed. Possibly the patterns could have resulted simply from subaerial and marine erosional exploitation of joint planes.
A list of these High islands is now given, arranged alphabetically and annotated. In reading the list, reference should be made to Charts 2764-, 2321, Aust. 101, 102...... » 8
ALBANY I. 10° W S. 142° 371 E. Macgillivray, 1852; sandstone cliffs 30’ high; Rattray, 1869, man, considered sandstone intruded by porphyry; Jack, 1881, 1892; Richards &
Hodley, 1925, say Albany Rock proves the unconformable relation of the sandstone to the quartz felspar porphyry* Photo* Plate 2*
Jardine, 1925, describes two benches; Jones & Jones, 1956, inter pret porphyry as either crystal tuff or ignimbrite, by analogy with Albany Rock, from which they examined a thin section* Prom
Rattray1s description I consider laterite caps the ? Blythesdale equivalent, which lies uneonformably on the porphyry* Aust, Pilot
IV, view p*208*
ALBANY ROCK. 10° 43! S. 142° 38» E* Jones & Jones, 1956
"ignimbrite overlain by Blythesdale Sandstone”; thin section figd.
PI* 2, figs. 1, 2.
BANKS I* 100 10ts. 1520 15! E. Rattray, 1869, "granitic";
Shepherd, 1944-* a c o m p l e x o f ro c k s o f gr a n i t i c type. T h e o ldest rock is a coarse grained normal granite, which has been intruded by a fine grained grey granite, a dark coloured quartz porphyry and a later and lighter coloured quartz porphyry* Wolfram occurs in lodes, usually associated with quartz porphyry. Fairbridge,
1950, fringed by sediment-covered reef with mangroves. Jones &
Jones, 1956, figd. thin sections, PI. 3, of quartz sericite schist and granite. Aust. Pilot III, view, p3 231.
BOOBY I» 10° 351 S. 141° 54*1 E* Moseley, 1892, porphyry.
Richards & Hedley, 1925, appears to be quartz felspar porphyry; emergence of a few feet suggested; two natural wells of fresh water near summit of island; photo. PI, 2, Jones & Jones, 1956, crystal tuff » 9
BURKE I. (a BOURKE I.) 9° 52’S. 143° 23* E. Rattray, 1869, granitic. Maitland, 1892, ’’appears to be granite”. Jones &
Jones, 1956, granite. Aust, Pilot, III, view, p. 204.
BUSH I. and TREE I. 10° 42’ S„, 142° 36» E, Richards (field notes 1925) "appears to be porphyry”.
CAP I. (= MUKWA) 9° 50’ S. 142° 43’ E. Haddon, Solías &
Cole, 1894.. "Jukes says its erroneously supposed to be volcanic ;
it is a bare mass of syenite”. Aust. Pilot, III, view, p« 204.
CORNWALLIS I. (- PAYAN = TAUAN I. = MT. CORNWALLIS).
9° 26’ S. 142° 32’ E. Jack, 1922, p. 363« Reported as granite,
by Moresby in "Baselisk" ; Haddon, Solías & Cole, 1894 "biotite granite; hornblende granite; and altered biotite aphanite or
diabase, appears to be pre-Devonian." Jones & Jones 1956 describe
a specimen of microgranite. Aust. Pilot, III, view, p. 231«
DEAD MAH’S I. 10° 34’ S. 142° 10 ’E. a tiny patch of rock on
the N. point of the fringing reef of Thursday I. Haddon, Solías
& Cole, 1894, altered quartz-andesite approaching rhyolite.
DOUBLE I. 10° 28*S. 142° 27» E. Jones & Jones 1956, granite
and aplite.
EAST STRAIT I. 10° 30’ S. 142° 27’ E. Jones & Jones 1956,
granite (pegmatitic and aplitic). Thin section figd. Pl0 2.
EBQRAC I. 10° 411 Sc 142° 32’ E. Rattray, 1869 porphyry
(matrix of felspar enclosing numerous crystals of yellowish quartz)
Richards & Hedley, 1925, quartz felspar porphyrye Jardine, 1925, benching at half tide, Pnotg Pl8 21. Jones & Jones, 1956 ignimbrite. 10,
ERNEST L ( a MC. ERNEST I- » NAGIR). Rattray, 1869, granitic. Macgillivray, quoted in Haddon, Solías & Cole, 1894,
”grey syenite0* Haddon, Solías & Cole say °has arkosic beach rock. More basic rocks also occur, e.g. altered augite-biotite aphanite and an altered ? basalt0. Maitland, 1892, ’’appears to be granitic”. Fairbridge, 1950, raised coral conglomerate$ section through island. FI. 25. Aust* Pilot III, views, p. 201, 204.
JlT 10° Q3* S. 142° 04* E. Rattray, 1869, ’’granitic”.
FLAGSTAFF I. (= WAIWIR) 10° 34’ S. 142° 11’ E. Haddon, Solías
& Cole, 1894, °Tuffs from eurites and granites”.
FRIDAY I. 10° 36» S. 142° 10* E. Richards & Hedley 1925,
”appears to be of porphyry”.
QABBA I* 9° 45* S. 142° 35* E. Maitland, 1892, ”appears to be granitic. Aust. Pilot III, view, p. 230.
GQQPE I. 10G 34* S. 142° 09* E. Flinders, 1814, ’’granite and porphyry with streaks of verdigris as if cliffs also contained copper.” (quoted in Jack, 1922). Richards & Hedley, 1925 »’appears to be porphyry.” Jones & Jones, 1956, ignimbrite and tuffaceous shales, etc. with acid to subacid dykes.
HAMMOND I. 10° 33* S. 142° 12* E. Jack, 1922, p. 132, contains auriferous quartz associated with copper pyrites. Richards
& Hedley, 1925, appears to be porphyry.
HAMMOND ROCK. 1(P 31* S0, 142° 12’ E. Jones & Jones 1956, propylitised rhyolite (or intrusive quartz porphyry).
HARVEY ROCKS. 10° 19’ S. 142° 41’ E. Jones & Jones, 1956,
Thin section iigd. PI. 1, fig. 4, ignimbrite.
HICKS I. (Cape York area). Morton, 1924, quartz porphyry as at C, Grenville and G. York. 11
HORN I. 10° 36* S. 142° 171 E* Savillc Kent, 1893, Photos.
Haddon, Solías & Gole, 18945 Jackson, 1902, map of part (of goldfield) porphyritic granite and quartzite of undetermined age, with felsite dykes. Fairbridge, 1950, fringing reef, sediment covered and with mangroves#
IDA I. 10° 42* S. 142° 33* E. Rattray, 1869, porphyry
(matrix of felspar, enclosing numerous crystals of yellowish quartz),
JERVIS I. (= MABÏÏIG) 9° 58* S. 142° 11» E. Haddon, Solías
& Cole, 1894, granite, rhyolitic tuff at Kwoims Hill. Qgilvie &
Weller, 1949, backbone of island of red granite.
MABADAUAN HILL (PAPUA). 9° 16! S. 142° 43* E. Haddon, Solías
& Cole 1894« MGranite rising out of Red delta plains of Fly R.,f
MAI I. 100 4 3 t s. 1420 37’ E. Richards & Hedley, 1925, quartz felspar porphyry overlain by sandstones. Jones & Jones,
1956; Thin section flaft. PI, 2 , figs. 3, 4, ignimbrite overlain by Blythesdale sandstone.
MX. ADOLPHUS IS. (5 MARI » YORK IS.) 10° 37* S. 142° 38» E.
Jukes, I 847, porphyry; Rattray, I 869, porphyry (matrix of felspars enclosing numerous crystals of yellowish quartz. Haddon, Solías
& Cole, 1894, all porphyry, varying from a softish base, apparently felspathic, with small transparent quartz crystals, to a hard siliceous base with flesh-coloured crystals of felspar. Richards
& Hedley, 1925, quartz felspar porphyry; photo, PI. 2, with a sandstone capping. Jack & Etheridge, 1892, p. 542, nearly hori zontal beds of sandstone, similar to those of Albany Pass.
MULGRAVE I. (= BADU). 10° 07» S, 142° 07» E. Shepherd, 1944,
’»a granitic complex including normal coarse-grained primary, 12 intruded by a fine grained grey granite, a dark coloured quartz porphyry and a later and lighter coloured quartz porphyry.
Wolfram in quartz lodes usually closely associated with porphyry.
Jones & Jones, 1956, granite (sheared at Kubin Village), a pro- pylitised andesite; thin section figd. P 1.2; also quartz mica schist, possibly pre-Gambrian.
POLE I. 10° 11»S. 142° 31*E. Rattray, 1869, granitic. Mait land, 1892, appears to be granitic. Aust. Pilot III, view, p.201, 204.
POSSESSION, I . 10° 43'S. 142° 24*E. Jackson, 1902, photo, map, a porphyritic granite, similar to that of Horn. I. Jack, 1922, p.625 refers to "Palaeozoic rocks, potentially auriferous, emerging from beneath horizontal sandstones of a later age."
PRINGE OF WALES I . (= MURALUG) Gaville Kent, 1893, photo..
Richards & Hedley, 1925, appears to be porphyry. Whitehouse (quoted by Jones & Jones, 1956) quartz porphyry. Fairbridge, 1950, fringing reef, sediment covered, with mangroves. Jones & Jones, 1956, Heath
Pt., ignimbrite.
RED WALLIS I. 10° 50»S. 142° 01*E. Jack, 1922, p.l65 quotes
"Beagle” as reporting as a conical hill of coarse sandstone*
SADDLE I . 10° 10*S. 142° 41 *E. Kaddon, Solías & Cole, 1894, of grey, fine-grained tuffs resembling sandstones with quartz fragments - a rhyolite tuff, not as coarso as at Habuig, but probably of same age.
Beach rock of coral fragments occur. Aust. Pilot III, views, p.201.
SAIBAI I. 9° 25*S. 142° 40 »E. Haddon, Solías & Gole, 1894 class this with Kawa, Borgu (Talbot) and adjacent islands Yarn,
Bobo (Bristow) and Parama (Bampton I.) as delta islands, low-lying, swampy, and wooded chiefly by mangroves. 13
THURSDAY I. 10° 35 ‘ S. 142° 14' E. Saville Kent, 1893 photo. Richards & Hedley, 1925, “appears to be porphyry“;
Fairbridge, 1950, flinging reef, sediment covered and with mangroves; p. 368, section through. Jones & Jones, 1956, rhyodacite interbedded with crystal tuff, shales with plant debris; thin sections, figd. PI, 1, figs. 1-3.
TUESDAY I, 10° 33* £ 3 42° 211 E. Richards & Hedley,
1925, “appear to be porphyry“,
TURTLE BASKED It 9° 54* S. 142° 46’ E. Jukes, 1S47, p. 156,
’sienite1; Rattray, 1869, “granitic“. Aust, Pilot III, view, p. 205.
WEDNESDAY I. 10P 30* S. 142019‘ E. Moseley, 1892, porphyry,
Richards & Hedley, 1925, “appears to be porphyry“.
YORK I. 10° 411 S. 142° 31* E. Seo Mfc. Adolphus Is,, porphyry. Aust. Pilot III, view, p. 308-9.
References to Geology of High Islands of Torres Straits
Australia Pilot III, 1950.
Fairbridge, 195-0 3
Flinders, 1814,
Glaessner, 1950.
Gray, 1928.
Haddon, Solías & Cole, 1894.
Jack, 1881, 1922,
Jack & Etheridge, 1892.
Jackson, 1902.
Jardine, 1925.
Jones & Jones, 1956. H.
Jukes, 1847.
MacGillivray, 1852.
Maitland, 1892.
Morton, 1924.
Moseley, 1892.
Rattray, 1869*
Richards & Hedley, 1925.
Saville-Kent, 1893.
Shepherd, 1944«
Whitehouse, 1955. 15
NEWER VOLCANIC HIGH ISLAN DS EA ST OF THE GREAT NORTH EA ST CHANNEL
East of the Great North East Channel and between 9 and
10°S* are a number of late Tertiary or Quaternary basic volcanic islands (largely olivine basalts) surrounded, or partly surrounded, by fringing reefs, and rising in general from about
10 fathoms of water over the continental shelf. (Jukes, 184-7;
Haddon, Solías & Cole, 1894-5 Mayer, 1915; 1918; Jack, 1922;
Jardine, 1925, 1928.) Whitehouse (1955) has compared these with the basalts of the eastern coastal ranges and valleys of Cape
York Peninsula and southwards, and considers they may have come up along a related crustal fracture or set of fractures. Some of them seem very young. Thus on Maer, a volcanic agglomerate contains boulders of corals of species still living. Glaessner
(1950) however compares them with the basalts of Norfolk Island and the supposed volcanic peaks, the submarine Tasmantides off the south-east coast of Queensland.
In using this* list, reference should be made to Charts
2764, 2321, Aus. 103. 16
BIACK ROCKS. 9° 9'S. U2° 48'E. Jardine, 1925, fig.; tuffs with a banded structure of corrso and fine grained material, dip S.W. 15°; on the north side, benches at high water mark; photo. PI. 19*
BRAMBLE CAY (= MASARAMKER) 9° ~#S. 143° 52 *E. Jukes, 1847,
"The reef is composed almost entirely of Heliopora coerulea:"
Haddon, Solías & Cole, 1894, a grey vesicular basaltic andesite,
Jardine, 1925, diagrami the volcanics are central to a large fringing reef with a cay of calcareous sand on its western edge, the sand almost entirely of foraminiferal tests, wit?i no pulverised material! the lava shows benching below
Jardine, 1928, map, photo. Pis. 6-7; basic lava flows and breccia, strike N* 30° W, varying to W. 10° N, dip 10° - 27° S.
CAMPBELL I. (= ZAPKER) near Murray Is. Haddon, Solías &
Cole, 1394* "since top of trees (105 ft.) is too high for a coral islet, it is presumably basalt".
DARN LEI I . (= ERUB) 9° 36» S. 143° 441 E. Jukes 1847, p. 154* P* 204; Maogillivray, 1852; Haddon, Solías & Cole, 1894; a mass of igneous rock, except in Treacherous Bay, where tuffs and agglomerates occur; the lava is a brilliantly fresh olivine basalt with a fluidal groundmass mainly occupied by plagioclase microlites and augite; photo of thin section, PI. 25; Jardine,
1928, Map» photos, Pis. 8-9»
MURRAY IS. 9° 54!S. 144° 03*E. Jukes, 1847, p- 154* 169*
204; Fairbridge, 1950, volcanic islets MAER (= MER), DAUAR (=
DONAR) and WALER (= WYER), surrounded by reef fringes with a
Lithothamnium ridge, without negro-heads; fig. 9, section through 17
Pt 368# Mayer, 1915, 1918, nLarge recently emerged shore- platforms about 3 it« above present high tide level; photos
Lenox-Conyngham and Potts, 1925, description and photos#
DAUAfi. according to Haddon, Solías & Cole, consists entire3y of ash, precisely resembling that of Mer; Dauar part of a different crater; MIffi. according to Haddon, Solías & Cole,
1894* "a great basaltic lava stream occupies the N.E* half; the horse-shoe shaped range to the S#W. is the margin of a crater of stratified volcanic ash with a quaquaversal outward dip of 30°; Photo, Pis# 23, 24; the basalts are marked by porphyritic crystals of olivine and monoclinic pyroxene, but groundmass is vitreous; in the ash, particles of foraminiferal and coral limestone are abundant, some crystalline, some dolomitised; photos of thin sections, PI# 25# WAIER, accords ing to Haddon, Solías & Cole, 1894 is of ash, but coarser than
Dauar and Mer, being agglomératic in many places; is half a crater; photo. PI# 23; thin section photo, PI# 25#
NEPEAN I # (= EDUGÖR) 9° 3 5 ,S. 143° 38*E# Haddon, Solías
& Cole, 1894* say nothing is known, but it is probably a mass
of basalt; Bligh called it a low woody island. 38,
References to Never Volce^aic High Islands East of the
Great North East Channel
Australia Pilot III, 1950,
Fairbridge, 1952*
Glaessner, 1950.
Haddon, Solías & Cole, 1894*
Jack & Etheridge, 1892,
Jardine, 1925, 1928.
Jukes, 1847.
MacGillivray, 1852.
Ma;*er, 1915, 1938.
Whitehouse, 1955* 19
A. II. THE SHELF FROM TORRES STRAITS SOUTHWARD TO SANDY CAPE
The Shelf widens noticeably from Princess Charlotte
Bay northwards, and from Trinity Opening southwards. The continental slope is steepest between 14° 30TS. and 16° S., where the Queensland Trench of 1000 fathoms or more lies only
2 miles from the outer barrier reefs* The slope gradually decreases southward from the Trench to about 22° S., where the Coral Sea Platform almost seems continuous with the shelf, only a very slight fall separating the two. Southward again it steepens quite remarkably as it closes in on Sandy Cape.
The known geology may be considered under that of the reefs, that of the high islands(north and south of Pt. Douglas) and that of the borings through two of its cays.
A ,II.d. The Geology and Distribution of the Reefs of the
Shelf between Torres St. and Sandy Cape.
Refer to Charts 2764, 2763.
The Queensland continental shelf varies a good deal in its width and the direction of its outer edge. As far south as the Bunker Group, it is studded with coral reefs that form a barrier to navigation in from the Coral Sea. The northern and southern halves of this barrier coral growth have very 20,
distinctive features possibly in part related to climate. The concentration of reefs other than fringing reefs and outer barrier reefs is gr at-st in the median (longitudinal) parts of the shelf, where patch reefs, the so-called ’inner reefs' of the Great Barrier, mostly without sand cays, rise from 20 to
25 fathoms# This zone of inner reefs in general widens and is found furthest from the mainland as one traces it southward.
It is separated from the fringing reefs of the coastline by the relatively clear inner or steamer channel, and in parts is separated from the line of outer barrier reefs by an outer channel 15-25 fathoms deep of relatively open water# The steamer channel is described by Fairbridge as forming a 15 fathom terrace, while he regards the ’inner1 reefs as rising from a lower 20-25 fathom terrace. He suggests that in places the
15 fathom terrace has intermediate steps at about 6-8 fathoms and 3 fathoms#
The shape of the inner reefs seems, as He/’ley & Taylor
(1908) and Fairbridge (1950) supposed, to be related to the form of the original feature on which they grew, and to the prevailing (wind generated) waves and currents. Thus if a reef grows on a submerged continental ridge or on a bank of sediment «¿ue ensign d Shelf end Coral Sea Features
The preen art 1 lue region! re-Ions of different development re^fs, north, and south of Trinity Orening. 21 elongated in the direction of current, it will retain this elongation throughout its life. If however it grows on a feature transverse to the prevailing waves and currents, its ends will recurve so that a crescent is formed with the horns down wind. The * inner reefs’ are, except for their western edges,
largely unsurveyed or unexamined. Some cays may H e on their
leeward edges, and only a few possess shingle ridges along the windward edges.
North of Trinity Opening (off Pt. Douglas) the edge of the con tinental shelf is the edge of the Great Barrier and lies in
general only 30 miles from the coast, which it roughly parallels to
C. Direction, whence it follows the 144th meridian, thus being
found at ever widening distances from the coast, which is stepped westward in a series of almost right angled bays. From Trinity
Opening northwards also, fringing reefs on the mainland coast and round the high islands are moderately well developed, though in
general now covered with mud and sand in their inner parts. Here also the outer edge of the shelf coincides with the outer edge of the outer reefs; inside the outer barrier the depth is usually
no greater than 30 fathoms; but outside, the floor falls away 600 -
1000 fathoms or more in 2-4 miles. Such a steep front to a Carrier
is found in the mobile area of New Caledonia and elsewhere (Spender,
1930). It could indicate fairly active downwarp here, at a maximum between 14°30’S. and 16°S.
The outer barrier reefs of this northern sector are linear or ribbon reefs, each 2-1$ miles long and 1000-1$00 ft. wide, separated by narrow openings half a mile in average width and no deeper 22, than the floor Inside the barrier* These outer barrier linear reefs have been well and often described; (Jukes, 1847;
Agassiz, 1898; Stephenson et al, 1931; Fairbridge, 1950); all save a few are awash at low tide; unvegetated sand cays above high water mark are known on some, in the section north of about
14-°S. but south of 12°S. are subject to destruction by cj^clones or storms, thus sanábanles Nos* 2-4- shown on early charts do not appear on the latest charts* Raine I. (11° 36’£.) on the outer barrier is considered by Jukes (184-7), Rattray (1856) and Fairbridge
(1950) to be an emerged reef, now undergoing erosion. It has a crust of strong calcareous sandstone and reef rock, of which a stone tower 64. ft. high was built by a party from R.M.S* »Fly1 that bivouacked for some months on the island. Its environs have been sounded in detail, the Raine I. entrance being at that time regarded as likely to be the chief entrance for traffic from tho Coral Sea.
In this vicinity a few great detached reefs rise from the slope outside the 100 fathom line, and great circular bays are found on the outer barrier; their origin is not understood. Raine I. lies north of the influence of most Queensland cyclones (Aust,
Pilot Vol. IV, p.38).
The orientation of the outer barrier reefs in the northern sector seems oblivious to the direction of the prevailing wind, but a current often sets parallel to the odge of the continental slope.
The ends of individual reefs are however curved inwards at the passages.
Fairbridge (1950) assumes that the linear reefs north of
Trinity Opening began as fringing reefs along an old Pleistocene 23
shore line where the sea level stood AO fathoms lower than now.
He postulates that this assumed Pleistocene shoreline was also
a fault scarp, due to pre-Pleistocene movement.
In this northern section the outer channel is some 15-25 fathoms
deep, and is cut into two by the junction of the inner reefs with the
outer barrier at either end of a 4-0 mile sector north of the One and-
a-half mile opening, but is represented within this sector by an
enclosed lagoon about 15 fathoms deep.
The inner reefs of the northern sector between C. Melville and
C. Direction show elongation N.E.-S.W., this direction corresponding
with the set of the tidal streams - (Aust.Pilot IV), but also with
the structural trends in the Flinders Islands (Fairbridge, 1950).
Fairbridge also suggests that the crescentic reefs between Cairns and
C. Bedford ori inated on N.E.-S.W. structural features "parallel" to
numerous (assumed) cross-faults on the adjacent mainland. None of
the inner reefs present any evidence of emergence. I think these
structural trend deductions very weakly based.
In the inner or steamer channel of the Northern half of the
shelf also, we find twenty or thirty low wooded island reefs, of
a type which is quite absent among the inner reefs, and is not
developed at all south of Trinity Opening. These are patch reefs
that dry at low water, and have a vegetated sand cay near their
leeward edge, vegetated shingle ridges or cays near their windward
edges and mangrove covered sand and mud flats. These low
wooded island reefs (Spender, 1930; Steers, 1929; 1930, 1931,
1937, 1938; Stephenson et al., 1931; Fairbridge, 1950) rise from
15 fathoms on the average, and are considered by most authors to
show evidence of a recent emergence of a few (?5) feet. Th^v 24- are elongated N.-S to N.N.W.-S ,S .Ë., the principal structural trend of the mainland as well as the main wind and current direction, so that the basement may be either a submerged continental island or a sedimentary bank (Fairbridge, 1950, p.363).
Contemporary sediment in this northern half of the shelf is dominantly terrigenous mud and sand along shore or on the fringing reefs; in the steamer channel just west of the low wooded island reefs it may be 64$ terrigenous or 36$ calcareous; to leeward of the island reefs the percentage of calcareous matter increases to
69$; and proceeding from the low wooded island reefs towards the outer barrier the percentage of calcareous matter rises to 64$
(Admiralty Charts; Jukes, 1847; Agassiz, 1898; Hedley & Taylor,
1908; Bryan, 1928; Steers, 1929; Marshall & Orr, 1931; Fair- bridge, 1950), Stream patterns from the main river mouths to the passages through the outer barrier cannot be traced, due, as Byran
(1928) has suggested to rapid sedimentation and to alongshore movement of sediment by currents.
South of Trinity Opening the Continental Shelf or its coral growths show many contrasting features to those noted to the north. Thus fringing reefs are relatively rare, and in general are found only on headlands. Low wooded island reefs are absent from the inner or steamer channel, which however retains its average depth of 15 fathoms only to about 18° 30'S., whence it gradually deepens and widens to become the Capricorn
Channel. The ’inner1 reefs of the northern section are however strongly represented on the southern section, and are found even further from the coast, and are even less well known.
Ribbon reefs of the type forming the outer barrier edge in the north, are not typically represented in the south, where the 25 outermost reefs lie some distance in from the 100-fathom line; this docs not fall very steeply or far on to the Coral Sea Platform, the Queensland Trench shallowing rapidly southward. Indeed in the southern sector, outer reefs and inner reefs become indistinguish able in form, being mostly irregular patches. Only two cays,
Bell Cay and Hixson Cay arc known on the Swain Reefs, though since they are largely unexplored and even unphotographed, more may exist.
Bell Caylies near the northern (leeward) edge of its reef.
Better known are the ’inner1 type reefs to westward of the
Capricorn Channel, forming the Capricorn-Bunker Group, spread over
150 miles, AO miles from the coast, Fairbridge (1950) considers that in these two north west-south east trending areas may be dis tinguished, one marked by Heron Is., Wistari Reef, Erskine I., Mast
Head I., etc., and the other by North-West I., built presumably on sedimentary trains running in at right angles to the shelf edge.
The N.W.-C.E. elongation of the individual reefs is taken to be due to the dominant currents running in this direction. These reefs mostly carry sand cays at their western, leeward ends, but Fairfax,
Hoskyn and One Tree I. reefs have shingle cays on their weather (S.E.) ends.
Part of the striking difference in development of the reefs north and south of Trinity Opening may bo due to present day climatic zones. In part it may be due to the greater amount of terrigenous material brought down by the larger southern rivers smothering coral growth there. Stanley (1928) suggested it is duo to Pleistocene coral growth having occurred only north of Trr.nity Opening.
For details of geology and references, see annotated list. 26*
The following is a list of authors on the geology of the cays and reefs :
Agassiz, 1398
Aust. Pilot III, 1950
Aust. P ilot IV, 1951
Chapman, 1931
Cushman, 1942
Edgcll, 1923
Fairbridge, 1950
Fairbridge & Tcichcrt, 1943
Haddon, Solías & Colo, 1894
Hedley & Taylor, 1909
Iredale, 1942
Jack, 1922
Jukes, 1347
Longman, 1913
Macgilliv r a y , 1852
Macgillivray & Rodway, 1931
Marshall, 1931
Marshall & Orr, 1931
McNeil, 1955a, b.
Moorhouse, 1933
Paradice, 1925
Rattray, 1869
Richards, 1928, 1938
Richards & Hedley, 1925
Richards & Hill, 1942 27.
Saville Kent, 1893
Spender, 1930
Steers, 1937, 1938, 1929
Stephenson ct al, 1931
Stubbings, 1938
Vaughan, 1917 28.
APPENDIX
TOPOGRAPHIC SECTIONS THROUGH THE QUEENSLAND CONTINENTAL SHELF huh. mmmom
See Charts 2764, 2763
Agassiz, 1898, Pis. 37 to 41.
1« From Elliott R. across Hervey Bay and beyond the continental
slope*
2. From Burnett Ro across Breaksea Spit.
3® From Kolan R. to Lady Elliott Island and beyond.
4. From Curtis Island through Masthead I., One Tree I., and
beyondo
5* From Port Bowen across the Capricorn Channelo
6o From Port Bowen across Swain Reef to Saumarez Reef and beyond*
7* From Broad Sound across the outer Barrier Reef to Marion Reef*
8a From Pt. Molle across Whitsunday I. to the Barrier Reef*
9® From Townsville across the Barrier Reef to Flinders Reef#
10* From Halifax B0 across the Palm Is. to Palm Passage* 11# From C* Grafton to Holmes Reef*
12* From C0 Grafton to Grafton Passage.
13* From the mainland across the Hope Is., Cairns Reef and Turtle Reef, to the outer Barrier Reef.
14» From Swinger Reef to Lark Passage*
15o From the mainland through Wooded I», the Three Isles, to the outer Barrier Reef*
16o From Lookout Pfc* to the outer Barrier Reef*
17o From Lizard I0 to Cormorant Pass®
18* From C* Flatteiy to S. Direction I* 19« From Brown Pk0 across Cole I. and Howiek I* to the outer Barrí,er Reef©
20© From C0 Melville to Melville Pass* 21* From Bathurst Pt. to the outer Barrier Reef* 22« From C0 Bowen through Bewick I. to the outer Barrier Reef* 29
23« From C* Grenville through the Blackwood Channel towards the Great Detached Reef.
24» From the Murray Is« in the direction of Flinders Entrance«
25o From Orman1 s Reef in the direction of Flinders Entrance*
26» From N« Warrior Reef to the N* end of Flinders Entrance*
27« From Mt« Adolphus to New Guinea*
28. From the mainland to Orman*s Reef*
Vaughan, 1917, p0 231 «
3« From Toowong Hill, S. Lat. 24° 22* 4 ,!, North 45° E« passing between Lady Elliott and Lady Musgrave Is*
4« From Rodd Peninsula, S« Lat« 24° 0* 0 % North 50° E«
5« From Georges Pt*, Hinchinbrook, B* Lat* 18° 25* 40”, North 72° 32* E*
Richards & Hedley, 1925«
1« From Lato 18° 28* 40US. long. 146° 19* 50« E. through Bramble, Trunk and Myrmidon Reefs*
Paradice, 1925« Sections from Long* 146° 22 * 34UE* to the 100 fathom line* 1. Along Lat. 17° 2* 48” S* through Hervey Patches to Outer Ridge*
2. Along Lat* 17° 4 1 54” S. through ridge extending N.E. from Noggin Reef*
3. Along Lat* 17° 8* 6nS. through Noggin Reef*
4« Along Lat. 17° 11* 30*lS. through Flora Reef, Coates Reef and Raaf Patches*
5« Along Lat* 17° 13* 42”S. through Hedley Reef.
60 Along Lat. 17° 18* 0n S. through Gibson and McCulloch Reefs*
7« Along Lat* 17° 19* 24n S. through Gibson Reef*
Fairbridge, 1950, p*368.
D e Through Thursday I«, Torres St* Reefs and Murray I. to Gulf of Papua.,
E« From C« Flattery through Li sard I* and longe Reef.
F, From C« Capricorn through Heron I* and Hixson C§r* 30,
BRAMBLE CAY (9° 7«S. 14-3° 52 >E) and SAUDI CAPS (24° 42'S. 153° 16'E_)
The list which follows is a catalogue of the references in literature that have any bearing on the form, origin or geology of the clastic accumulations built above high water mark on the coral reefs of the Gréa-*' Barrier« Some reefs without banks of clastic accumulation are recorded because their shape is significant in the argument concerning the types of platforms on which reefs grow« In using it reference should be made to the charts cited for each entry0
A,TTGH ffp T O P renamed HELSDON Reef, quo vide«
ANCHOR CftY (on outer barrier) 9° 22*S* 144° 06!E« Aust«
Pilot III, p«170« A bare sandbank near the north-western end of a reef, at the northern most termination of the Great Barrier reef35 Fairbridge, 1950, po340, unvegetated sand cay« Aus© 103«
ARDEN I. (Torres St.) 9° 52!S. 143° 10'E. Aust, Eliot III, p«201« .Wooded, 50 ft« high to tops of treec$ has a light tower on north west edge of reef j (being so low, this island is probably a sand cay)| Macgillivrsy, 1852, vol«2, p©42, a quarter of a mile long, low and sandy$ on the W® edge of reef, AuSo 103«
AELINGT.QH REEF 16° 40»« 146° 00!. Aus Pilot III, p„197.
Has UP0LÏÏ sand cay, vegetated and 8ft© high at its N«W* end®
Stephenson et al, 1931, akoiSo Steer3, 1937, po14, some vegetation©
Steers, 193% Po 68, of cay© Fairbridge, 1950, p«345, a crescentic reef platform, po349, with characteristic vegetated sand cay© Chart 2350©
ATJRE3D I. 9° 58«S. 143° 17'3. Aus. Pilot III, p.201 „ Low, wooded fringed with reefs (probably a sand cay, D.H. ) Aus« 102o
BATT REEF. 16° 25*S. 145° 4 5 !E. Aus« Pilot IV, p©231e
Stephenson et al., 1931, p.29, man ; description p©30; uncovers only at spring tides. Fairbridge, 1950, airphoto. Pl«1, fig© B©, diagram, p©358; a patch reef without island* ^hart 2924*
BEANLEY ISLETS (on pauch reef) (BEANLEY and INGRAM ISLETS)
14° 26*So 144° 53 !E« Steers, 1937, p.19j 1938, p«84 Map?
Beamley is a vegetated shingle ridge (ranpart), Ingram is a vegetated sand cay, Fairbridge, 1950, p©349, sand cay, reef- flat and ramparts vegetated© Chart 2922e
BEAVER GAY. 17° 50*S. 146° 30*E. Richards, 1928, p«xiv; this sand cay was found to have moved \ mile between two success ive surveys; consisted of loosely coherent coral detritus unvegetated. Steers, 1929, p* 248, map; movement was 100 yards in a fortnight« Chart 2349#
BEE (B) BEEF. 15° 38*S. 145° 26*Ea Agassiz, 1898, Photo pi. V; a long flat sandy islet with a conical heap of coral debías at the S© end of the reef flato Hedley & Taylor, 1908, p.*397 Section
Spender, 1930, p*285, vegetated sand cay, unvegetated rampart and flat5 Steers, 1937, p*130, Fairbridge, 1950, p©286« Chart
2923,
BELL CAY 21° 46'S. 151° 16:E. (in Swain Reefs). Aus. Pilot
IV, p»56c A small sand cay near the northern edge of its reef,
scantily vegetated; there is an anchorage off the N© side about ir mile from edge of reef, in depths of about 20 fathoms, but bottom is hard and uneven; about 200 yds© long; spring tides rise 16 ft* Fsirbridge, 1950, p© 341 © Chart 346© 32 ,
~~'OTCK I. (on patch reef). 14° 26'S. 144° 49'E. Steers,
1937, p.124, a low wooded island, described; Steers, 1938, p.82 map of island on reef; Fairbridge, 1950, classed as sand cay,
reef flat and ramparts, vegetated* Chart 2922*
BIHSTEAD I. (CLAREMONT GROUP). 13° 13'S. 143° 34'E. View
Aus* Pilot IV, p*277; 10 ft* high with some stunted trees, on
N*E* edge of reef. Steers, 1937, a low wooded island* Chart
2921*
BOURNE ISLES (Spelt BOURKE on Aus. 103) around 9° 50*S.
143° 25*E. Aus Pilot III, p*201, all wooded and fringed with
coral reefs (LAYOAK, AUKANE, KABBIKANE and BOURNE), (presumably
sand cays, D*H.). Aus* 103*
BOYD PNG CAYS. 11° 35*S. 143° 02»E. Aus. Pilot IV, p*299
Fringing reefs, some with islets on them; e.g* BÖYD0NG I0, a
low wooded island* Haddon, Solías & Cole, 1894, p*466, Chart 2919*
BRAMBLE REEF (Palm Passage). 18° 24'S. 146° 41'E. Agassiz,
1898, Photo, pi. 12; Richards & Hedley, 1925, section through;
Chart 2349.
BURKETT I. (Claremont Group) 13° 56,S. 143° 45TE. Steers,
1937, low wooded island; Steers, 1938, ran of sand cay only,
Chart 2921.
CAIRNCRQSS ISLETS. 11° 14'S. 142° 55'E. Rattray, 1869,
regarded them as elevated coral islets* Aus* Pilot IV, p»302,
on northern part of reef; tops of trees 85 ft. Chart 2919*
CATRWB REEP. I 50 40'S. 145° 30'E. Agassiz, 1898. photos
pis* XIII - XV, nothing but a mass of negro heads of all sizes
forming a belt along the W* edge of the reef. Hedley & Taylor,
1908 section, p.397 nformerly had a central lagoon which is being filled 33.
inP Fairbridge. 1950, airphoto pl«5, fig. C. a l,nea3vatolln$
10 miles long, p.345, a horseshoe reef platform, diagram p. 358, grew convex to prevailing S.E. wind, horns pointing down wind.
Chart 2923o
CAMPBELL ISLET (= TAPPQEAR). 9° 34!S. 143° 29!E« Aus.
Pilot III, p.200, low wooded, tree-tops 48 ft., shown on Aus.
103 as long and spitlike, up the centre of a N.E. trending reef.
Haddon Solías & Cole, 1894, remarked that CAMPBELL I. (=ZAPFER), having a height of 1 ft0 is probably basaltic, though they did not visit ita Nothing certain is known of its constitution.
Aus« 103.
CEE (C ) REEF See Cowlishaw Reefo
CHAPMAN REEF with unvogetated sand cay, 12° 53!S 143° 36!E.
Aus© Pilot IV, pc281, islet, 500 yards long N. and S«, 200 yards broad, vegetated, Steers, 1937, p.126, described, main islet is of shingle banks (ramparts), on E0 of reef. Steers, 1938,* p.95, mao showing snail sand cay, unvegetated, on N.W. edge of reef and main islet of ramparts on E.
CTACK REEF 14° 03*Sa 144° 16^. carries sand cay with mangroves on NeE0 edge; Steers, 1937, pd31o Chart 2922.
COATES PEEF 17° 12*S. 146° 22*E, Paradice, 1925, Airphoto frontispiece; chart and soc^pjj; a horseshoe reef. Chart 2350®
DOQOMUO a 10° 35So 143° 4*E. Aus Pilot III, p®202, low woode’d, on northern side of reef; tops of trees 51 ft®, coc canut palms 76 ft*. Aus0 1021
'14° 24*3. 144° 54!E„ Aus. Pilot IV, pe256, a sand CQ.jp vegetated, on Wo end of reef0 Steers, 1929, p®248, man® Chart 2922* 34.
COQUET I. 14° 33!S. 145° 33«E. Steers, 1937, p.123, described; Steers, 1938; Fairbridge, 1950, sand cay reef flat and ramparts all vegetated. Chart 2922,
CQWLISHAW (= CEE (C)) REEF. 15° 32«S. Agassiz, 1898, p,ll6, only a sand patch, Fairbridge & Teichert, 1948, almost completely submerged reef, Fairbridge 1950, p,357, an initial patch reef. Chart 2923,
DALKYMPLE ISLET (= DAMUTH). 9°37«S. 143° 18«E. Aus, P ilo t III, p,200. Low, wooded, at N.W, edge of reef, with light tower and native village. Aus* 103.
DAVTF. REEF, 13° 58« S. 144° 27«E. Fairbridge, 1950, p.340, airphoto, pi, 5, fig. A. "annular in form with a sand flat and shallow pools, apparently an infilled lagoon". Chart 2922,
DAWSON REEF (previously DEE «D« REEF), 15° 30«S. 145° 19’E. Agassiz, 1898 "only a sand patch11, Fairbridge & Teichert, 1948, p.85f almost completely submerged reef. Chart 2923. DAY REEF 14 30« S. 145 32«E. North of Cook«s Passage,
Fairbridge 1950, airphoto pi, 3, fig. B (not named). Chart 2923, DHU (D) REEF. See Wharton Reef, DOVE ISLET (= ÏÏTTU). 10° 00«S, 143° 02«E. Aus. P ilo t I I I , p.201, low, wooded Aus, 102,
DUNGENESS I , on Dungeness Reef, 9° 48*S. 143° 6«E. Aus, Pilot III, p,201, flat, swampy and densely wooded; Aus. 102.
Ee (E) REEF- See Egret Reef.
EAGLE REEF, 18? 51*S. 148° 05!E. Agassiz, 1898, photo pi, 16, p.122, a low coral sand islet, vegetated; a line of
sand bars along edge of reef. From anchorage in 7 fathoms,
discoloured coral sand with terreginous detritus. Chart 348, 35
EAST CAY. 9o 24»S, 144° 12!E., Aus. Pilot III, p. 170, a low sand cay on the N.W. end of a cluster of reefs.
EDDY CAY. 17° 46* S, 146° 28^. > previously marked on charts, on reef near BEAVER GAY, has been washed away (Steers,
1929, p.251). Chart 2349. EF (F) REEF. See Forrester Reef. EGRET REEF (formerly Ee Reef). 15° 29«S. 155° 25«E. Fairbridge, 1950, p.358, an initial patch reef; diagram,
ELLIS I. 13° 22« S. 143° 42«E. Aus. Pilot IV, 6 ft. high. Steers, 1937, p. 16, a sand cay with beach rock; in 1936 no vegetation was seen, being recently destroyed by a cyclone. Chart 2921,
ELLISON REEF. 17° 43'S. I 460 25* E. Fairbridge, 1950, p.345, a crescentic reef-platform. Chart 2350, ENN I . See Nymph Island.
ERSKINE I. 23° 30»S. 151° 46«E. Steers, 1937, p.9, a sand cay, Steers, 1938, p.59, Map of cay only , wooded, with beach rock. Fairbridge, 1950, p.366, suggests this (with
Wistari Reef, Heron I. Masthead I, etc.( lies on a N.W. - S.E. trending sedimentary train, running in at right angles to the shelf edge. Aus. I 6I.
ESCAPE REEF. 15° 50«S. 145° 45‘E. Spender, 1930, p.281 lies half a mile within the 100 fathom line, but is an outer barrier reef. Chart 2924.
FAIRFAX I . 23° 5VS. 152° 23«E. Macgillivray and Rodway I 93I, three wooded islets, connected by reef at low tide, small supply of brackish water; some goats; guano previously worked, 36 now a waterhole. Steers, 1937, largest islet in N.E., of cemented shingle; middle of shingle ridges; smallest a sand- trail from middle islet, but separated from it by a cyclone. Aus. l 6 l, FARMER and FISHER ISLETS (in the PIPER I s .) 12° l6 *S . 143° 14*E. Steers, 1937, p.120, low wooded islands, one a sand cay, the other wooded shingle ramparts. Chart 2920.
FIFE I. (on patch reef). 13° 39* S. 143° 43'E. Steers,
1937, p.15, map, vegetated sand cay, the reef on which it stands is a mere sand flat over large areas on its lee side. Steers, 1933, p*91, map showing sand cay only, on W. edge of reef,
Fairbridge, 1950, p.349, vegetated sand cay on reef. Chart 2921, FITZROY REEF. 23° 37'S, 152° 9*E. Vaughan, section through from Rodd’s Peninsula, criticised in Richards & Hedley, 1925, p .25, Steers, 1937, p.10, a reef enclosed lagoon with no island, there is a narrow gap in the reef for entry to the lagoon in good weather. Aus. I 6I, FLORA REEF. 17° l l rS. I 460 18»E. Paradice, 1925, p.57, chart, and section. Chart 2350.
FORRESTER REEF, formerly Ef (F) Reef. 15° 10'S. 145° 30*E. Agassiz, 1893, p.117, one huge mass of coral left standing as i t grew, 9 f t , high, 250 yds. inside edge of reef, is regarded as evidence of elevation. Fairbridge, 1950, p,359, a horse hoof
shaped patch reef, a mile or two in diameter, diagram, p.358.
Chart 2923.
GIBSON REEF. 17° 18'S. H6° 22'E. Paradice, 1925, p.57
chart and section. Chart 2350. GREEN I. (on patch reef). 16° 46'S. 145° 58«E. Steers,
1929, largest sand cay on reef, photo 4. Steers, 1937, p.15 37 reef more isolated than others with sand cays, and not just on the margin of the Barrier; vegetation thick. Fairbridge,
I95O, airphoto, pi.6, figs. A, B., p.349. a tourist centre, (hart 2350.
HALFWAY I. Torres St. 10° 7*S. 143° Í9*E, Aus. Pilot III, p.201, wooded. Flinders, quoted by Jack, 1922, says this is a key only a few feet above spring tides. Aus. 102,
HAM and DERRY REEFS near Second 3-mile opening, 13° 03' S.
143° 53fE. are outer barrier reefs, each with a sand cay 2 ft, high on its western edge. Chart 2920, 2921,
HANNAH I. (Claremont Group). 13° 15 1S. 143° 43*E. Steers,
1937, p.128, photo. low wooded island. Chart 2921,
HANNIBAL IS, 11° 36»S. 142° 56*E, Bligh (quoted by Jack,
I922, p.101) refers to this as a key. Chart 2354,
HARDY, HOOK, BAIT and LINE REEFS. 19° 45< - 19° 50’S.
149° 15fE. Edgell, 1928, p.52, chart p*54. Fairbridge, 1950,
calls Hardy & Bait, two complete atolls, and Hook and Line two
near atolls open to N.W. - all rising from 30 fathoms. Chart 348.
HARRIER REEF. 15° 08'S. 145° 41'E. Aus. Pilot IV, p.343,
lies just inside Lark Pass through the outer Barrier, and has
small sand cay on N, side (not shown on Chart 2923, 1952 Reprint).
HASTINGS REEF. 16° 30'S. 146° l'E. Fairbridge, 1950, p.357
an initial patch reef with two horns down wind, diagram p.358
Chart 2924.
HAÏ I. (Claremont Group). 13° 41'S. 143° 41'E. Steers, 1937,
p. 136, photos. low wooded island described on p.127; traces of
emergence, p,25. Chart 2921.
HEDLEY REEF. 17° 13fS. 146° 29'E. Paradice, 1925,.p.52,
chart and section. Chart 2350. 38
HELSDON REEF, formerly Aitch (H) Reef. 14° 57«S. 145° 30*E.
Fairbridge, 1950, p.359, a small oval patch reef. Chart 2923* HERALD PATCHES (in Swain Reefs). 24° 13«S. 152° 42«E. Aus, Pilot IV, p.56, says 4 of the Herald Patches lie along the inner edge of the Great Barrier Reefs in a N.W. trend from
Howard*s Patch, Aus* I 6I. HERON I. 23° 26« S. 151° 57*E. Aus, Pilot IV, p.52,
springs rise 10 ft. Jukes, 1847, p.6 described beach conglomerate
Photo in Sav ille Kent, 1893, p i* 30B. Steers, 1929, p.243 reports the Lightship from Breaksea Spit drifted to here. Steers, 1937, a shallow lagoon (6 ft.) on reef flat. Steers, 1938, p,6l map of cay only, wholly of sand, with beach rock on S. Richards, 1938, p.135, account of boring. Richards & Hill, 1942, description of bore core (see appendix No. 1 to my Report for details of this boring), to $08 f t ., the bore passed through reef rock with two intercalations of terrigenous sands; from 508 to 732, through dominantly incoherent terrigenous sands with a calcareous phase between 636 and 702 f t . Cushman, 1942, p.112, foraminifera from the bore; Iredale, 1942, p.120, mollusca from bore. The bore appears not to have penetrated through Recent and sub-recent sediments, Fairbridge, 1950, p.366, considers the reef built on sedimentary train elongated ESE-WNW due to currents in that direction; a vegetated sand cay. Aus. I 6I.
HERVE! SHOALS. 17° 03* S. I460 28*E. Paradice, 1925, p*60, chart and section. Chart 2350.
HIXSON CAY (in Swain Reefs). 22° 21»S, 152° 40*E. Saville
Kent, 1893, an in sign ifican t sand patch. Aus. P ilot IV, p.l49> a sandy islet on the outer edge of the reefs. Most southerly 39. known cay of Swain Beefs. Fairbridge, 1950» p.368, section through. Chart 346.
HOPE IS. 15# 4 4 ’S. 145® 28‘E. Aus. Pilot IV, p.234 two sandy cays 28 ft. high, vegetated. Macgillivray, 1852, p.104, description: Agassiz, I898, photo, pi.VI. Steers, I929, P*252 sand cay on one reef, mangroves and shingle cay on other, photo 5 *
Steers, 1937> p.130 described? changed since Hedley & Taylor’s visit in 1906. Section Spender, 1930, p.209> diagram on p.206.
Steers, 1938, Map of cay and shingle on reefs (W. Hope I and E
Hope I.). Fairbridge, 1950, E. reef is crescentic. Chart 2923.
HOSKYN I. (Bunker Group). 23° 4 8 !S. I520 l8’E. MacGillivray and Bodway, 1931» p.58, 2 parts, wooded, connected at low tide by reef. Steers, 1937> small N.E. island of shingle ridges; large S.W. island also of shingle; possible evidence of erosion of a former island. Steers, 1938, p«57> Map showing position of 2 parts on reef. The small E. island is exceptional for the
Capricorn and Bunker Groups, where islands usually on S.W. end of reef. Aus. I6l.
HOUGHTON I. (on patch reef). 14° 31'S. 144° 58'E. Steers,
I929, gives description p.255? photo 11; Steers 1937» P«25 says evidence of emergence in presence of higher platform of marine erosion, 10-11 ft. above L.W.M., and 8-9 ft. above r.ief level, description p.123* Steers, 1938, p.8l Map of cay and ridges on reef. Stubbings, 1938, description of gravel and sand fragments
(coral and shale) from sample 1^ feet down. Fairbridge, 1950, p.349; sand cay, reef flat and ramparts vegetated. Chart 2922.
HOWIE BEEF. 17° 23’S. 146° 24*E. Fairbridge, 1950, chart on p.365; a windward crescent reef, 7 miles lohg, facing ESE, 40 rising on S.E. from 25 fathoms* In W.N.W. is a smooth platform of 2-5 fathoms 2 miles wide, with coral heads; a steep scarp leads down to another platform at II-I7 fathoms, extending 2 miles leeward. Chart 2350*
INGHAM I. (See BEANLEY I.). Steers, 1937, phetos. Steers
1938, Map.
JUBILEE REEF 13° 10'. 143° 46'E. Aus. Pilot IV, p.2T9, with a sand cay and boulder 6 ft. high on its northern end.
Chart 2921.
KAY (= K) ISLET. 12° 13»S. 143° 16'E. Aus. Pilot IV, p.291 a vegetated sand cay on the N.W. edge of the reef. Chart 2920.
KEATS I. (Torres St.) (=UMAGU, HOMOGAR) 9r 41*S. 143° 26»E
Haddon Solías & Cole, 1894» p.452, a sand cay 1/3 mile long on
N.W. edge of reef. Aus. 103*
KEY/ IS. See Pethebridge Is.
KING I. 14* 6'S. I44® 20'E. Steers, I929, p.255, shows good shingle rärnjarts; Steers, 1937, p.124, described as low wooded island. Steers, 1938, p.86 Map of sand cay only. Fairbridge
I95O, p.349, sand cay, reef flat and ramparts vegetated. Chart
2922.
LADY ELLIOTT I. 24° 7*S. 152* 43* E. Jukes, 1847, descrip tion. Macgillivray, I852, low, of coral formation. Photo in
Saville Kent, 1893,-pi* 33* Steers* 1937, P*7, 1938, p«53, Map island V3 mile long, V4 mile wide, of cemented coral shingle.
Some guano. Fairbridge, 1950, P*349, a moderately stabilised shingle cay on reef. Aus. 161.
LADY MUSGRAVE I. (No. 1 Islet, Capricorn Group). 23° 54’S
I520 24’E. Steers, 1937, p.6, island of cemented coral shingle, with a lagoon; some guano. Steers, 1938, p .56 ^aP showing 41.
island on reef. Stubbings, 1938, p.97> lagoon gradually-
being filled in with sand 5$ quartz, 95$ calcareous materials
molluscan fragments, corals and foraminifera; coralline algae
rare. Fairbridge, 1950, p.345, an ’atoll1; has lagoon 4-5
fathoms deep; a moderately stable shingle cay on reef, p.349*
Aus. 161.
LARK PASS, unnamed outer barrier reef 5 miles to N. of
15° 01*S, 145° 4 3 ’E. Fairbridge, 1950, pl*3, fig. A. airphot?
Chart 2923. Photo of reef near, Saville Kent, 1893, PI.12.
LARK PASS, unnamed outer barrier reef, S. of 15° 08*S.
145° 4 4 ’E., Agassiz, 1898, description; Fairbridge, 1950, p«340.
LAYOAK ISLET. 9e 52’S. 143° l8 ’E. One of Bourne (Bourke)
Is. Low, wooded, 56 ff« fo top of trees. Aus. Pilot III, p.201.
Aus. 103.
LONG I. (= SASSIE) 10° 0 2 ’S. 142° 50*E. Aus. Pilot III,
p.202. Swampy in parts, densely wooded, tops of trees II4 ft.
Aus. 102.
LOW ISLES. 16° 23’S. 145° 34’E. Site of Great Barrier Reef
Expedition, much photographed and described in detail. A typical
low wooded island, its characteristics related to wind and tide.
Macgillivray, I852, p.101, description. Steers, 1929, p.252,
Photos 6, 7. Spender, 1930, p.195, reef processes; coloured map;
photos. Marshall & Orr, 1931, contemporary sedimentation.
Stephenson et. al. 1931 Map, Photos, description. Moorhouse,
1933, p.35, 37, map, photos, effect of cyclone. Steers, 1937,
P.119, is furthest south of low wooded islands; description, p.135«
Fairbridge & Teichert, I948, p.67* Map, photo, reef processes and
changes since 1933* Fairbridge, 1950, airphoto pi. 7, sand cay,
reef flat and ramparts vegetated, p.349* Chart 2924. 42
LOWRIE I. (Claremont Group). 13° 17»S. 143° 36'E. Steers,
1937> p*127, a low wooded island. Chart 2921.
LOWWOODED I. 15° 5'S. 145° 23'E. Aus. Pilot III, p.240,
View C, Photo Saville Kent, 1893, PI.13? 15-17« a typical low wooded island, described Steers 1937» p.124. Steers, 1938, p.74,
Map of island only. Fairbridge, 1950? P*349? sand cay, reef flat and ramparts, vegetated. Chart 2923«
McCULLOCH REEF 17 17‘S. 146 28'E. Paradice, I925, p.60, chart and section. Chart 2350.
MACKAY REEF. 16° 3'S. 145° 4 1 *E. Aus. Pilot IV, p.231, has a sand cay 4 ft. high near western edge, reported to be partially vegetated and to be conspicuous, in 1929« Steers,
1929, p.249? Steers, 1937? P«14? in 1928 covered with vegetation in higher parts5 in 1936,. beginnings of new cover of plants| probably the 1934 cyclone practically destroyed the cay. Steers,
I938, map of cay only. Fairbridge, 1950, P«349? unvegetated sand cay. Chart 2924«
MAGRA ISLET. 11° 52«S. 143° 17*B. Aus. Pilot IV, p.297, a sand cay with bushes on it on the N. end of a detached reef near the W. side of Cockburn Reef. Chart 2920.
MARSDEN ISLET (Torres St.) (= EEGARBU). 9° 43,S. 143° 21’E.
Aus. Pilot III, p.200, low wooded, near S. edge of reef. Aus.103«
MARTHA RIDGVAY REEF. 12° 10’S. 143° 4 7 ’E., an outer barrier reef in a large indentation (Y/reck Bay) in the Barrier, described
Jukes, I847? p.122. Chart 2920.
MASTHEAD I. (Capricorn Group). 23° 33’S. 151° 44TE. Aus.
Pilot IV, P.53? on W. edge of oval reef. Hedley, I9O6, p*453> description. Longman, 1913, plants. Edgell, 1928, movement of oay. Steers, 1937? p.10, a sand cay with dunes. Steers, 1938, 43 p.5Ô, Map of cay only? beach rock on S. side. Fairbridge, 1950, p.360, seems with Heron I, Erskine I. and Wistaria Reef to be on a N.W.-S.E. trending sedimentary train, running in at right angles to the shelf edge, suggesting the dominant currents run in N.W. and out S.E. Aus. I6I.
MICHAELMAS CAY. 16° 36’S. 145° 59'E. The site of a boring by the Great Barrier Reef Committee. Aus. Pilot III, p. . a sand cay 8 ft. high, covered with vegetation at the western end. Marshall, 1931, p .66, a calm-water:reef. Chapman, 1931, p.32, list of forams in bore samples. Steers, 1937, p»14j
Steers, 1938, p. 68-9, map of cay only. Richards, 1938, p.138, reference to bore. Richards & Hill, 1942, p.72, description of bore core samples. For full details of the bore samples, see
Appendix I to my present report. The boring determined reef rock with little terrigenous matter dominated to 378 ft., inco herent grey green glauconitic and calcareous quartz foraminiferal
sand to 6OO ft., basement not reached. Fairbridge, 1950, p*349
et al, discussion of significance of boring. Chart 2924«
MORRIS I. 13° 2 9 ‘S. 143° 4 3 ’E. Aus. Pilot III, p.273,
8 ft. high,covered with coarse grass and bushes, on the western.
edge of the reef. Steers, 1937, a vegetated sand cay, with some
planted sisal hemp. Chart 2921.
MYRMIDON REEF. 18° 15»S. 147° 22»E. Richards & Hedley,
I925, F»l, large scale cross section of shelf and reefs between
this and Hinchinbrook I. Chart 2349*
NEPEaN ISLET. (= ATTAGOY) in Torres St. 9° 34'S. 143° 39’E.
Aus. Pilot III, p.199, says tops of trees 62 ft. This seems low 44* for a basalt island, as thought by Had don, Sollar «Sc Cole, 1894 nothing certain known. Aus, 103.
NEWTON I, (on patch reef), 14° 30»S 144° 55'E, Steers,
1937, p.128, a low wooded island, Fairbridge, 1950, p.349, sand cay, reef flat and ramparts vegetated. Chart 2922.
NIGHT I. (on patch reef), near C, Direction, 13° 11'S.
143° 34’E. Steers, 1937, p.120, low wooded island, closer to mainland than any other; description p.122. Steers, 1938, p.92,
Map of islets on reef. Fairbridge, 1950, p.349, sand cay, reef flat and ramparts vegetated. Chart 2921,
NOGGIN REEF,. 17° 8»S. 146° 29'E. Paradice, 1925, section and chart. Chart 2350,
NORTH REEF in Capricorn Group. 23° ll'S.. 151° 54'E Steers,
1937, a small sand cay with low bushes has fomed near W. end.
Aus. 161.
NORTH WEST I . . 23° 18'S, 151° 42'E. MacGillivray and Rodway,
1931, p.58, largest island of Bunkers and Capricorns, 400 acres.
Steers, 1937, p* 9, a sand island.. Steers, 1938, p.64 Map of cay. only; has guano,. Fàirbridge, 1950, p.366, seems with Heron I,
Erskine I. and Wistaria Reef, etc. to lie on a N.W0-S,E. trending sedimentary train, running in at right angles to the shelf edge, and suggesting the dominant currents run at right angles to the coast here. Aus. 162.
NïMPH I. (Formerly En (N) I.) on patch reef. 14° 39'S. 145°
15*E . . Steers, 1937, p.125, described as standard low wooded island; p.19, ridges of coarse shingle at heights and in situat ions remote from present wave action but closely related to beach awash at high water; traces of higher platform 3 ft, above the 45. lower. Steers, 1938, p.79, map of island on reef. Fairbridge,
1950, p.349, classes as sand cay, reef flat and ramparts vegetated. Chart 2922.
ONE TREE I. in Capricorn Group. 23° 30*S. 153° 08* E.
Jukes, 1847, p.4. Steers, 1937* photos; perhaps most exposed of all in the group; of coral shingle entirely, in original ridges; Steers, 1938, p,60, Map of shingle cay only, close to weather (S.E.) edge of reef. Fairbridge, 1950, p.349 a moderate ly stabilised shingle cay on reef. McNeill, 1955, p.333, 404, photos. Aus. 161.
PANDORA ENTRANCE, vegetated sand cay on outer barrier reef on S.E, side of, 11° 26*S. 144° OO’.E, Aus. Pilot III, p.167,
6 or 7 ft. high. A chain of sand cays, each surrounded by a reef, extends nearly 10 miles N. and S, lying 10 or 12 miles westward of the entrance, the northernmost and largest slightly vegetated. Chart 2920,
PELICAN I. 13° 55'S. 143° 50'E. MacGillivray, 1852, p.113, low, sandy, I/4 mile long, on N.W. edge of reef. Steers, 1937, p.15, vegetated sand cay on sandy reef: Steers, 1938, p.90,
Map of cay only, Fairbridge, 1950, p.349. Chart 2921.
PETHERBRIDGE IS. formerly KEW (Q) Is. 14° A 4 ’S. 145° 6>E.
Steers, 1937, p.130. Steers, 1938, p.77, map of V». Kew I. on reef; beach rock is exposed and an old sand cay is completely eroded from inside it. Fairbridge, 1950, p ?349. sand cay, reef flat and ramparts vegetated. Chart 2922.
PICKERSGILL REEF. 15° 52fS. 145° 34'E. Spender, 1930,p.285 sand cay 3 ft. high on N.W. end unvegetated, but previously vegetated., Steers, 1938,p,71. map of sand cay and sand bank only. Stubbings, 1938, p.97, a lagoon in centre of reef> 46 gradually filling in; Fairbridge, 1950, p.343* map from air photo, diagram p,358; a lagoon atoll, unvegetated. Chart 2924»
PIPER IS. 12° 1$«S. 143° 14*E. Aus. Pilot IV, p.290,
4 wooded islets on 2 dying reefs. Fisher & Farmer Islets, each about 45 ft. high, are situated on S.W. and N.W. ends respectively of the eastern reef. Baird Islet (40 ft.) and
Beesley Islet (a vegetated sand bank 6 ft. high), are situated on the eastern and western ends respectively of the western reef.
Rattray, 1869* p.304, grouped with Raine I, Caimcross and
Howick Is. Chart 2920.
PIPON I. (on patch reef). 14° 8'S. 144° 31'E. Reports, Gt„
Barrier Reef Committee, vol.2, frontispiece, photo of niggerhead.
Stefrs, 1937* p.121, low wooded island. Steers, 1938, p.85 map of islets on Reef. Fairbridge, 1950, p.349* sand cay, reef flat and ramparts, vegetated. Chart 2922.
PIXIE REEF. 16° 33'S. 145° 52’E. has a sand cay 1 ft. high on its northern end. Chart 2924.
RAAF SHOALS. 17° 11'S. 148° 33'E. Paradice, 1925, p.60 chart and section. Chart 2350.
RAINE I. 11° 36'S. 144° 01* E. Jukes, 1847* p.126, detailed description, a plateau rising 25 ft, above Low Water Mark (or perhaps 13 ft. above H.W.M.) of calcareous sandstone, an elevated reef island, figure p.127» plan p.338, section p.339. Guano. A naval surveying party from H.M.S. ’Fly’ bivouacked on the island, evidently for some months, building from blocks quarried on the ■ island a circular stone tower 64 ft. high: Rattray, 1869* p.303* an elevated coral island. Fairbridge, 1950, p,341* an isolated reef platform with offshore slope of 45° - 55°; it exposes cores 47 pr platform of older coral material; there is no evidence of a continental core, hence Steers (1929) was wrong in calling it a ’continental ’ island. This outer barrier island is definitely a possibility for a boring site. The chief difficulty would be navigation, but a detailed chart (2354) exists, and directions in Aus. Pilot III. A view is given on chart 2354* D.H
Chart 2354*
REDBILL I. and BUSHY I. on REDBILL REEF. 20° 57'S. 150° 5'E
Aus. Pilot IV, p.126, Redbill is 93 ft. high is thus probably continental; near western edge of reef on which Bushy I (40 ft.), a vegetated sand cay, lies. Steers, 1937> Bushy I, p.13, a sand cay; Steers, 1938, p. 66, Map of Bushy I., a sand cay with beach rock on the W. Chart 347.
RENNEL I. (- MAUAR). Torres St. 9° 46'S.. 143° 16'E. Aus.
Pilot III, p. 200, wooded, 72 ft, to tops of trees, lies on N.W. edge of reef. Has a village. Aus. 103.
RIBBON REEF 14° 45'S. 145° 42'E. a typical outer barrier reef, Spender, 1930, p.31. Fairbridge, 1950, airphotos, pi.2, figs. A, B, diagram (by Whitehouse) p.339. Chart 2923.
ROBERTS I. 9° 59'S. 143° 7'E. Aus. Pilot III, p.201, low wooded island, 50 ft. to tops of trees. Aus. 102.
RUBY REEF. 15° 45*S. 145° 47fE. Spender, 1930, p.281, 283 an outer barrier reef somewhat protected by Anderson Reef which lies to windward of it on the southern side of Papuan Pass.
Chart 2924.
SANDBANK Mo. 1, 14° 12'S 144° 53'E. Aus. Pilot III, p.158,
Cay on Outer Barrier, 2 ft, high, on western edge of reef forming
S. side of Waterwitch Passage, Chart 2922. 48.
SANDBANK No. 2. 13° 59>S. 144° 30 *E. Aus. Pilot III, p.159, cay on Outer Barrier, 8 ft. high, on western side of lÿdema^s Reef, q. v. Not shown on 1954 reprint of Chart 2922,
SANDBANK No. 3o 13° 59* S. 144° 26»E. Aus. Pilot III, p.
159, cay on Outer Barrier, 7 Ft. high, on western edge of Davie
Reef, q. v. Not shown on 1954 reprint of Chart 2922.
SANDBANK No. 4. 13° 5 j *S. 144° 21«E. Aus. Pilot III, p.
159* 6¿ miles W.N.W. of Sandbank No. 3, a sand cay, not shown on 1954 reprint of Chart 2921,
SANDBANK on outer barrier at 13° 47*S. 144° 17* E* a small dry cay, shown on 1953 reprint of Chart 2921,
SANDBANK No. 3* on outer barrier at 13° 42*S. 144° 43 E,
Aus. Pilot III, p.159, a dry sand cay a few feet high. Chart
2921.
SANDBANK No* 6, an outer barrier at 13° 38* S , 144° 0 5 ’E*
Aus. Pilot III, p.159, Chart 2921.
SANDBANK No. 7* on outer barrier at 13° 26‘S. 143° 42!E. on reef on north side of Firct Three Mile Opening. Aus. Pilot
III, p. 159, Chart 2921.
SANDBANK No. 8. on outer barrier at 13° 22’S. 142° 43»E.
Aus* Pilot III, p.160, is vegetated. Chart 2921.
SAND CAY ON HAM REEF on outer barrier, near 13° 03*3,143° 33*E.
2 ft, high. Chart 2921.
SAND CAY ON DERRY REEF on outer barrier, near 13° 03*SC 143°
53*E 2 ft, high. Chart 2921.
SATELLITE REEF. 16° 26* S. 145° 41*E. Stephens*::?, et al
I 93I, p.29, on Map with Batt Reef. Chart 2924*
SHERRARD I. (Claremont Group), 12° 59* S, 1 4 3 ° 37 »E,
Steers, 1937.. P»16, a low wcrded island, mangrove just beginning 49 to colonise. Steers, 193S> p* 94* map cay and shingle islets on N, end of reef, beach rock without enclosed cay visible further south, Stubbings, 1938, p.97* description of foraminif*- eral sand from sand cay. Chart 2921,
STAPLETON CAY, 14° 19* S* 144° 50»E* 19 ft. high* Steers,
1929/ p«74* 248* map: Fairbridge, 1950, p,349> a vegetated sand cay. Chart 2922.
SUDBURY REEF, 16° 57'S. 146° 09 ’E. with unvegetated sand cay, 6 ft, high, on N.W. end of reef. Steers, 1937* photo, p,14*
Steers, 1938, p.67, map of unvegetated sand cay only. Fairbridge,
1950, p,349. Chart 2350.
SUE I. (Three Sisters Group, with Poll and Bet Is,),
10° 12'S, 142° 50’E. Jack, 1922, p,264* coral sand, wooded.
Aus* Pilot III, p, 202, 3. Aus, 102,
SWAIN REEFS at southern end of Barrier. Has two known cays, Bell Cay and Hixson Cay, quo vide. Jukes, 1847* p*15.
These consist of a compact body of coral masses, intersected by narrow channels of deep water; each mass varies in extent from one to several miles, some of them being almost dry at low water, others having lagoons or hollows of greater or less depth, A very ccrrnon feature among them is a line of great detached blocks lying a little back from the outer edge of the reef, frequently not altogether covered even at high tide and always quite exposed at low water. These negroheads have been t o m off and thrown up on to the re.ef during storms. Jukes gives a summary on p,321,
Fairbridge, 1950, p,363, section through to C. Capricorn. Chart
346.
SWINGER REEF, 15° 15TSo 145° 32'E. Agassiz, 1Ö98, p.122,
"a small sand cay has formed in it since the time of the last 50.
survey." Aus. Pilot IV, p.243, sand cay, 3 ft, high, on NiW,
end of reef. Chart 2923«
THREE ISLES. 15° 07*S, 145° 25*E. MacGillivray, 1852, p.105, description of low wooded island, Agassiz, 1898, photos, pi. 7-11« Steers, 1929, p«256, detailed description. Spender,
1930 p.204, photos detailed description, coloured map« Stephenson
et al 1931, photo. Fairbridge & Teichert, 1948, P«76, shows long shingle tongues, Fairbridge, 1950, sand cay, reef flat and ramparts, vegetated. Chart 2923«
TORRES STRAITS REEFS. Haddon, Solías & Cole, 1894.
Fairbridge, 1950, p.346, boat-shaped, E.-W, orientation due to
currents; p, 368, section through.
TONGUE REEF. 16° 23»S, 145° 46'E. Stephenson et al., 1931, p.29, S.W. end on map with Batt Reef, Chart 2924.
TRUNK REEF. 18° 21'S. 14-6° 50'EC Richards & Hedley, 1925, section through via Bramble Cay and Myrmidon Reef. Fairbridge,
1950, a crescentic reef platform. Chart 2349«
TRYON I, 23° 15*S. 151° 47'E. Steers, 1937, p.9, a sand cay with dunes 30 ft, high. Steers, 1938, p.65. Map of cay only,,
Beach rock on S, Aus. 161,
TURTLE GROUP, 14° 56*S, 145° 03'É. Six islands and a few
reefs, Agassiz, 1898, p,ll6. Steers, 1929, p.255, description.
Steers, 1937, P« 128, low wooded islands on reefs. Steers, 1938, p,?8, map of one islet only, on its reef, Fairbridge, 1950, p.249 sand cay, reef flat and ramparts vegetated, Chart 2923«
TWO ISÏES. 15° 01'S. 145° 26'E, MacGillivray, 1852, p.106, description of low wooded island6 Steers, 1937, p«131j Steers,
1938, p e 75, map of cay and ramparts on reef. Fairbridge & 51
Teichert, 1948* p.76, ’long shingle tongues’, Fairbridge, 1950, p, 349, sand cay, reef flat and ramparts vegetated. Chart 2923*
TYDEMAN REEF. 13° 59'S. 144° 31’E. Fairbridge, 1950, p.340, airphoto, pi, 5, fig. A, annular in form, with a sand flat and shallow pools, apparently infilled lagoon. Chart 2922,
UNDINE REEF with vegetated sand cay. 16° 07’S, 145° 40’E,
Cay 3 ft, high near western edge. Steers, 1937, no vegetation in 1936, Steers, 1938, ,p.69. Map of cay only. Fairbridge,
1950, p.349. Chart.2924.
UPOLU CAY. See Arlington Reef,
VICKING REEF formerly V. Reef, 11° 36’S. 143° OO’E. Jack,
1922, p.101 reports that Bligh said it had two sandy keys on it.
Today (Aus. Pilot III, p,299) these are awash at high water.
Chart 2919.
WARRIOR I. (- TUTTE, TOD) 9o 48'S. 142° 58>E. Aus. Pilot
III, p,205, view; p.201, a vegetated sand cay on a reef, with a native village. Haddon, Solías & Cole, 1894, a sand bank.
Chart 2422. Photo in Saville Kent, 1893, pis, 11, 13.
WATSON I. 14° 28'S. 144° 54'E. Steers, 1937, p.128. Cay carries no vegetation that can be detected with glasses, some beach rock, however; shingle islets with usual mangroves,
Fairbridge, 1950, p,349, sand cay , reef flat and ramparts vegetated. Chart 2922,
WHARTON REEF foimerly Dhu Reef (D). 14° 08’S, 144° OO’E. with sand islet 2 ft, high on western end, shingle islet on N,E9 end, vegetated. Steers, 1937, photo, p,120, description. Steers,
1938. Fairbridge, 1950, p.349, sand cay, ramparts and reef flat, vegetated. Chart 2922.
WILKIE I. (Claremont Group), .13° 47’S. 143° 38»E, Steers, 52. 1937, p.l29, low wooded island. Steers, 1938, p.89, Map, sand cay, reef flat and shingle ramparts all vegetated. Chart 2921.
WILSON REEF. 13° 57'S. 144° 24'E. Fairbridge, 1950, p*340, airphoto. pi.5 fig.A, annular in form, with a deep lagoon; is a true « shelf atoll. Chart 2922.
WILSON ISLAND. 23° 18'S. 151Ô 55*E. Steers, 1937, p.8 photos, on small reef, consists of a mass of coarser and finer material| doubtful if sand predominates over shingle; excellent beach rock on weather side. Steers, 1938, p.63, Map of cay only. Au3. 161.
WISTARI REEF. 23° 2 8 «S. 151° 52'E. Photo in Saville Kent, 1893, pl.30B. Steers, 1937, p.10, sometimes has evanescent sand bank.
Fairbridge, 1950, p.366, "seems (with Heron I., Erskine I., Masthead I., etc.) to lie on a north west-south east trending sedimentary train, j running in at right angles to the shelf edge. Most of these reefs are oriented N.E. S.W. to E.-W., suggesting the dominant current in this broad part of the shelf runs at right angles to the coast. Aus. 161.
WRECK I. 23° 20’S. 151° 57'E. Jukes, 1847, p.ll, described vegetated sand cay. Steers, 1937, p.9* Steers, 1938, p.62, Map of cay only; beach rock on S. Aus. 161.
YONGE REEF. 14° 36'S. 145° 38'E. A typical outer barrier reef.
Spender, 1930, photos, pis. 11, 12, 14; sketch fig. 9. Description.
Oblique (N.N.W.-S.S.E.) to trade winds, which have no visible effect on the ribbon form; debris scattered over the surface without forming a cay or rampart. Stephenson et al, 1931, Map, p.31, description, only accessible at low spring tides, Photos Fairbridge, 1950, p.339, diagrammatic sketch. fig. 2; diagram by Whitehouse, p.339; section through, p.368. Chart 2923.
YORKE IS. (MASIG and KODALL). 9° 45 lS. 143° 25!E. Haddon,
Solías & Cole, 1894, p.452, sand cays, wooded, on reefs. Aus. 103. 53.
A. II.e. THE HIGH ISLANDS AND HEADLANDS BETWEEN CAFE YORK
AND PT. DOUGLAS.
Refer to Charts 2354, 2920, 2921, 2922, 2923, 2924
The islands about and to the north of C. York, as already noted
above in Section A.I.b are related to the rocks of the northmost part of C. York Peninsula.
The groups of islands off C. Grenville (Cockbum I., Sunday I.,
the Home Is., Clarke Is., Haggerstone I., Sir Charles Hardy Is. and
Forbes Is.) are of granite, or of quartz felspar porphyry (which in
Clarke I. at least is regarded as ignimbrite by Jones & Jones 1956,
but different from that of the Torres St. Is.) or of felstone
suggesting highly siliceous lavas affected by contact metamorphism.
Those off C. Weymouth and C. Direction (LloydI., Restoration I. and
Rook and Rockyl.) are granitic, like these Capes. These islands
are geologically similar to the headlands off which they lie, and
could well be parts of the probably Palaeozoic igneous masses found in
Chillagoe Shelf region and the Hodgkinson portion of the Jack Basin.
The Flinders Group of Islands off Bathurst Hd. in Princess
Charlotte B. and Clack Island just to the north, are of ?Jurassic
sandstones, arched into an elliptical dome with its longer axis
N.N.E.-S.S.W. These sandstones are evidently a continuation of
the Jurassic freshwater sandstones of the Laura Basin.
The next geological grouping of islands (Howick, the Lizard
Group, Saddle and Eaglet Isles) lies off the coast between C. Melville
and C. Flattery, and is of Palaeozoic granite, ...... 54
like much of the rock of the coastline between these two
capes, while Rocky Islet off Archer Pt. is like that headland,
of the Lower Palaeozoic Barron R¿ metamorphics characteristic of
the North Coastal structural High.
Fringing reefs are common, but none of the islands show
barrier reefs, unless the Lizard la. reefs be interpreted as such.
Most of these islands lie close to the coast and to the west
of the steamer channel, but the Sir Charles Hardy Is., Forbes I.,
Howiek I. and the Lizard Isles with Eaglet and Saddle Islets lie within the inner barrier reefs, so that in their immediate vicinity there is unlikely to be any very great thickness of marine strata under the shelf.
From Archer Pt. to C. Grafton, high islands are few.
F6r details of geology and references see annotated list
(pp.67).
The following authors have written on the geology of these
islands and headlands:
Agassiz, 1898
Aust. Pilot IV, 1951
Fairbridge, 1950
Haddon, Solías & Cole, 1894
Jack, 1881, 1922
Jack & Etheridge, 1892
Jardine, 192$
Jones & Jones, 1956
Jukes, 1847 55.
MacGillivray, 1852
Morton, 1924
Rattray, 1869
Richards, MS.
Richards & Hedley, 1925
Shepherd, 1936
Spender, 1930
Steers, 1929, 1937, 1938
Stephenson et al, 1931
Whitehouse, 1955 56.
EAST COASTAL HEADLANDS OF C. YORK PENINSULA AND HIGH ISLANDS
BETWEEN 11° SOUTH AND PORT DOUGLAS
ARCHER PT. 15° 36'S. Jardine, 1925, coarse and fine grained quartzites and banded slates traversed by quartz veins strongly folded and crumpled, strike varies from E.30°N. and
N.35° W, and dip from 82° S.E. to 75° N.E; diagram p.H7$ a wave-cut bench 4-8 ft. above H.W.M. Steers, 1929, photo 9, of lower bench. (Probably Barron R. metamorphics, D. Hill).
BOLT HD. 12° 15'S. Jack, 1881 and 1922, p.568; a bare promontory which presents a cliff of about 100 ft. in height to the sea for -J- mile. At the top of the cliffs are about
30 ft. of horizontal reddish sandstone (? laterite or ?Blythesdale sandstone, D.H. ) resting unconformably on a blue limestone with a quasi-schistose structure (?Chillagoe Silurian-Devonian D.H.)
The limestone was at least 100 ft. thick, and had a dip to the E. at 45°.
C.- BATHURST. 14° 15'S. Rattray, 1869, a bold cliff of sandstone overhanging the sea, like that of the adjacent Flinders
Is. (? - Walloon, D.H.) Whitehouse (1955) and Jones & Jones
(1956) interpret these as Blythesdale Sandstone.
C. BEDFORD. 15° 13'S. Jack 1881, an isolated fragment of the commoner masses of horizontal sandstone of the Peninsula.
As seen from the sea, the Desert Sandstone forms a small isolated tableaux perched on slaty rocks at about 400 ft. above sea level.
(Jurassic on Barron R. metamorphics. D.H.)
C. BOWEN. 14° 31'S. Jack; 1881 and 1922, p.150. The bare hillside shows 3 thick horizontal beds of sandstone, separated by 57.
soft beds, presumably of shales, and resting on what appear from a ship to be highly inclined schistose rocks. (Jurassic on Barron R. Metamorphics. D. Hill.)
G. DIRECTION. 12° 50'S. Jukes, 1847, granite; Rattray,
1869, granitic; Richards & Hedley, 1925, granite.
C. FAIR. 12° 24»S. Rattray, 1869, granitic. Richards
& Hedley, 1925, granitic mass.
G. FLATTERY. 14° 58»S. Jack 1881 and Jack & Etheridge,
1892, p.530. A great thickness of gently undulating Desert
Sandstone beds comes down to the sea in places, and in others highly inclined schists were seen underlying the sandstone in the sea cliffs. Here the lower third of the sandstone is of brown sandstone and shales, and the upper two-thirds of white sandstone; Steers, 1929, photo. a high island tied to the mainland by a tombolo; bench just below H.W.M. cut into much contorted and metamorphosed Palaeozoic rocks, and still more
(in the northern part of the Cape) in Mesozoic sandstone and
conglomerate. Fairbridge, 1950, p.335, fringing reef; p.368
section through Reef. (Barron R. Metamorphics with Walloon
freshwater sandstones above. D.H.)
C. GRENVILLE. 11° 57*S. Jukes, 1847 in Jack, 1922.
“Highgate Hill nearby is of a brown siliceous rock passing
into porphyry, as in the Sir Charles Hardy Is. Morton, 1924,
fine to medium grained quartz porphyry. Richards & Hedley, 1925,
granitic mass.
C. MELVILLE. 14° 0 9 ’ S. Jukes, 1847, p.99 granite;
Macgillivray, 1852; Rattray, 1869, granitic. Jack & Etheridge,
1892, p.530 !,as seen from the sea consists of apparently a 58.
thickness of three or four hundred feet of Desert Sandstone coining down to sea level or slightly undulating. Morton, 1924» granite weathering into huge rounded boulders as in the Pascoe
R. area. Richards & Hedley, 1925, granite. Steers, 1929, photo of granite weathering into huge rounded boulders. Fairbridge,
1950, almost uninterrupted fringing reef, mostly sediment covered, varying in width from 3,000 to 3,000 ft. stretching between C. Melville and C. Flattery.
C. WEYMOUTH. 12° 38'S. (near Iron Range). Rattray, 1869, granite. Richards & Hedley, 1925, granitic mass. Shepherd, 1936, granite from the Iron Range belt of schists to the coast at C.
Weymouth, map.
C. YORK. 10° 41'S. Macgillivray, 1852, porphyry;
Rattray, 1869, laminated porphyry (matrix of felspar enclosing numerous crystals of yellowish quartz.) Rattray reports Osnaburg,
Bishop and Ida Pts. near C. York also of this porphyry.
(Probably the post-Lower Carboniferous pre-Mesozoic porphyry as in the Pascoe R. area D.H.)
CLACK ISLAND at S.E. corner of Clack Reef. 14° 5'S. 1 4 4 ° 1 5 ’E.
Richards & Hedley, 1925, quote Cunningham on 'Bathurst1; it consists of coarse granular siliceous sandstone 1 6 - 2 0 ft. thick at base, in which are large pebbles of quartz and jasper; above this is 10 ft. horizontal stratum of soft black schistose rock, and above this sandstone. Richards & Hedley sav baa hnin cliff over 140 ft. high of sandstone dipping gently North, and think it continuous with the ? Jurassic sandstones of the Flinders Group.
CLERKE IS. 11° 58'S. 1 4 3 ° 18'E. Richards & Hedley, 1925, quartz felspar porphyry of fine grained flinty type; Jones & 59.
Jones, 1956, ignimbrite, different from that of Torres St. Islands.
COCtiBURN IS. 11° 50»S. 143° 20» E. Haddon, Solías & Cole,
1894. Dark »felstone» with a marked fluidal structure on weathered surfaces, suggesting highly siliceous lavas affected by contact metamorphism, photo of thin section, PI.25.
RACLE ISLET. 14° 42»S. 145° 23'E. Rattray, 1869, crystalline.
FALSE 0KF0RD NESS. 11° 23«S. Jack 1881 and 1922, p.593,
is a low promontory of horizontally bedded red sandstone coming
down in a cliff to the sea. The Ness is covered (lightly near
the sea) with blown sand, which accumulates inland into high
sandhills. These extend inland for 2 or 3 miles till they abut
on a range of heath-clad sandstone hills. p.604> from False
Orford Ness to Orford Ness low points of sandstone come down at
intervals to the sea. Sandhills cover the sandstone, and front
the bays between the headlands.
FLINDERS GROUP. 14° 12»S. Richards & Hedley, 1925• Five
in numberj are composed of sandstone, very rugged, with stunted
trees and scrub! Map, text-fig., p.4. The sandstone is probably
Mesozoic, a continuation of that on Bathurst Hd., and which over-
lies porphyry in Cape York Peninsula; represents a foundered
region that once extended as a Cape north from Bathurst Hd.
A denuded anticline has its axis (probably N.N.E.) in the Owen
Channel! Section. Fig. 3> photo. Pl.l. The anticline plunges
to N.N.E.-S.S.W. Folding considered post-Tertiary. Sandstone
current bedded, conglomeratic at base, micaceous above; pebbles
in conglomerate were chert, hornfels, jasper and quartz with no
granite; the sandstone just over the conglomerate is coarse and
free of mica; higher up it micaceous and grey. A metamorphic 6 0 . and granitic source to the East is suggested. No shales.
Much limonitic replacement of sandstone. No fossil wood, but fresh water origin suggested. Total thickness 700 ft. A raised rock platform, 4 ft. 6 ins. above present, occurs.
Whitehouse (1955) interpreted as Blythesdale. (? Jurassic
Walloon equivalents? D. Hill).
FORBES IS. 12° 18'S. 143° 25'E. Rattray, 1S68, «granitic*
Richards 1925 notes, granitic.
HAGGERSTONE 1. 12° 02'S. 143° 18»E. Richards 1925 notes, granitic. Jones & Jones, 1956, granitic.
HARDY IS. (= SIR CHARLES HARDY IS.) 11° 55'S. 143° 28*E.
Rattray, 1869, granitic. Jukes, 1847, a brown siliceous rock, like a flinty slate passing into porphyry.
HOME IS. (East of C. Grenville). (See CLBRKE I .)
HOWICK I. (in Howick Reef) 14° 2 8 *S. Richards 1925 notes, granitic. Steers, 1938, partly of granite.
KING I. 14° 5'S. 144° 2 0 'E. Richards à Hedley, 1925,
Sandstone, no doubt fragment of once continuous terrain from
Flinders Is. and C. Bathurst. Steers, 1938, however maps as low wooded island reef.
LIZARD GROUP. 14° 40*S. Jukes, 1847, granite; Rattray,
1869, granitic. Agassiz, 1898 photos PI. 16, 21, 22; Richards
1925 notes, granitic. Steers, 1929, practically uncliffed;
Spender, 1930, photo of N.W. Bay; Stephenson and others, 1931.
map; granite; photo ; description. Fairbridge, 1950 fringing reef.
LLOYD I . 12° 46*S. 14 3 ° 2 3 'E. Richards 1925 notes, granitic.
LOOKOUT PT. 14° 50*S. Richards & Hedley, 1925, old meta-
morphic rocks exposed in cliff faces along coast up to and a
little beyond Lookout Pt. 61
ORFORD NESS. 11° 18*S. Richards & Hedley, 1925, say not examined, appears to be relatively low lying sandstone cliff.
See False Orford Ness.
REMARKABLE RED CLIFF. 11° 12»S. Jack & Etheridge, 1892, p.542, shows two coal seams, each a-quarter inch in thickness in the midst of red sandstone. (Blythesdale Sandstone, D.H.)
RED CLIFFS. 11° 49’S. Jack, 1922, p.619, sandstone
( ? Blythesdale Sandstone or Latérite, D.H.).
RESTORATION ISLAND and RESTORATION ROCK. 12° 38»S. 143° 26'E.
Richards & Hedley, 1925, on R. Rock, acid aplitic granite with
E.-W. joints dipping S. 70° - 80°, and N.S. joints dipping E. at
45°. Crossed by basic porphyry dykes. R.I. a coarser granite,
? porphyritic orthoclase, reddish when weathered.
ROCKY I. 12° 55'S. 143° 33'E. Richards 1925 notes,
aplitic granite.
ROCKY ISLET. 15° 37'S. 145° 20'E. Jones & Jones, 1956,
Barron R. metamorphics, interpreted from a specimen and from
Richards 1925 notes, "very highly metamorphosed slate which
indicates fairly intense pressure and possibly contact
metamorphism.n
SADDLE ISLET. 14° 4 1 ‘S. 145° 27 *E. Jones & Jones, 1956,
granite and ignimbrite.
SUNDAY I. 11° 56»S. 143° 13’E. MacGillivray, 1852, p.118
of flesh-coloured felspar; Rattray, 1869, ditto.
TEMPLE BAY. See Bolt Hd. and Wreck B.
TURTLE HD. 10° 56'S. Richards & Hedley, 1925, not examined
but appeared to be relatively low-lying sandstone cliff.
WRECK BAY (l mile S. of Bolt Hd.). Jack, 1881 and 1922,
p.568; the bare headland just S. of the wreck is of horizontal 62. sandstone (Blythesdale, D.H.), resting on serpentine, about
100 ft. in height. (Mid-Devonian ? D.H.)
YULE PT. to PORT DOUGLAS. 16° 35‘S. Fairbridge, 1950, p.333* extensive fringing reefs, edge 1000-2000 ft. offshore, almost entirely covered with terrigenous mud. Daily spring tide range 10 ft. 63. A.H JC. THE HIGH ISLANDS AND HEADLANDS BE.SESI PT. DOUGLAS AND SANDY CAPE.
Charts 2350, 2349, 348, 347, 346 and 345 should be used in conjunction with this section
From Archer Pb. to C. Grafton high islands are few and their geology is not known. Off C. Grafton are the Fitzroy Is.,, g ran itic lik e th a t cape. Between C. Grafton and Hinchinbrook Island lie High I. and several groups of islands, the Frankland Is« (Normanby and Russell), the N. Barnard Is. (Egg, Jessie, Kent, Lindquist, Rocky I.) S. Barnard Is. (Sisters and Stevens),
Dunk I., the Family Group, and Brook Is. which are either granitic or gneissose, like the headlands Rocky Pt., Cooper Pt., Flying Fish Pt., Hilda Hill and Tam o!Shanter Pfci These are eitheï* granitic or gneissose, and Jones & Jones, 4r>56, regard the gneisses as Pre-Cambrian, forming cores of anticlines in Barron R. Lower Palaeozoic matamorphics. The age of the granite is unknown. All these islands l i e quite close to the coast, west of the steamer channel. Many of them show N.N.W.-S.S.E. alignment, with the grain of the country.
The Palm Is. (Great Palm, Fantôme, Pelorus, Orpheus, etc.) are granitic, but the age and relations of the granite are unknown. These islands show fringing reefs, but the development of fringing reefs becomes le s s around the high islands as one works southward along the shelf. Magnetic I. close to Townsville and C. Cleveland are of
granite intrusive into Permo-Carboniferous volcanics.
From Ce Upstart (granite) to the eastern shores of Broad
Sound, the islands nearest the coast are e ith e r of Upper Palaeozoic 64 volcanics or of intrusive granites; evidence of age of any of these volcanics is known only in the vicinity of Pt» Newry where Leoidodeqdron australe indicating an upper Devonian or Lower Carboniferous age has been found. These islands are, from N. to S», Holboume I», of granite, rather isolated and some distance offshore; the islands of Edgecumbe Bay (Stone I», Middle I», Poole and Thomas Is», Gloucester I» with Passage Islet, and islands of the Whitsunday Passage and Whitsunday Group, like Rattray, Eshelby, Hayman, Saddleback, Langford, Black, Armit, Olden, Gumbrell, Double Cone, Hook, Grassy, Border, Deloraine, Whitsunday, Dumbrell, Ireby, Cid, Molle (N» & S.) Edward, Harold, Haslewood, Dent, Hamilton, Lindeman, Seaforth; the Cumberland Group including Shaw, with Brushy Rock and Yellow Rock, Boynham, Comston, Keyser, Maher, Mansell, Pine Isle t, Thomas and Triangle Is» and the Sir John Smith Group; the islands of Pt» Newry, including the Newry Is», Acacia, Mausoleum and Redcliff» The small Wedge I» off C» Hillsborough, like the Cape, 'is of Tertiary bedded volcanics with freshwater shales. Further off shore, Cockermouth Island is of rhyolite of suggested Tertiary age, while Scawfell I. is of granite» These two are tentatively grouped with the Percy Is. and the Duke Is. in a different structural region from the Whitsunday groups above, and which w ill be mentioned shortly. Coming southward from Pt» Newry among the near shore islands, one meets Flat Top I» of granite with f el sitie dykes, and passes on to the porphyry headland of West H ill, and on the W» coast of the E. side of Broad Sound, Long I. also of porphyry. These three are tentatively correlated with the upper Palaeozoic 65. volcanics and granites o f the Whitsunday Group.
Cockermouth and Scawfell Is. with the rhyolites of the
Percy Is., are tentatively grouped with the limestone and tuffaceous strata of the Duke Group (Hunter, Iron, Marble and
Morter), which contain early Devonian coral reefs. The next
group o f islands whose geology is known, is the Keppel Group in Keppel Bay. These, Arch, Peak, S plit, Divided, S. Keppel,
N* Keppel, Middle and ^rall Is . are a ll o f quartzites, e tc. o f the Lower Palaeozoic Brisbane Metamorphics, while B luff Rock,
Creek Rock, Double Head and Bluff Pt. are all of Tertiary trachytic necks. Most of the strikes on these islands are
the regional N.N.W. strikes.
Curtis I. and the northern end of Facing Island, together with the small islands of Ft. Curtis (Compigne, Picnic, Quoin,
Tide and Turtle) are o f Lower Palaeozoic Brisbane Metamorphics, with the regional N.N.W. strike. But Gatcombe Hd., at the
south-west o f Facing I . , exposes ? Pre-Cambrian metamorphics
presumably in an an ticlin al core.
Duck I . and Woody I . in Hervey Bay, are o f Lower Cretaceous
marine shgQ.es.
For details of geology and references see under individual
islands and headlands in the accompanying annotated l i s t .
The following authors have contributed to the geology of
these islands or headlands î
Agassiz, 1898
Andrews, 1902
Aust. Pilot IV, 1951
B all, 1904
Bryan, 1936 66 «
Airbridge, I95O
Hedley, 1925
Henderson, 1931 Jack & Etheridge, 1892
Jardine, 1925, 1928
Jones & Jones, 1956
Jukes, 1847 Lenox-Conyngham & Potts, 1925 Maitland, 1892
M arshall, Richards & Walkom, 1925
Rainford, 1925
R attray, I 869 Richards, MS*
Richards & Hedley, 1925 Saville-Kent, 1893
Stanley, 1928
Steers, 1929, 1930, 1937, 1938 Sbo Smith, 1918, 1919
Vaughan, 1917 67. mmw LIST .OF .HIGH .ISLANDS AND HEADLANDS ETC. .OF THE QUEENSLAND COAST BETWEEN PT. DOUGLAS AMD BREAKSEA SPITJŒQSEJiEQL^
ACACIA I . 20° 5-2^Se 148° 55!E« U. Dev, or LoCarb* sediments and volcanics, with ? Jurassic sandstone. Chart 347,
ABMIT IS. 20° 6*S. 1480 39fE. Stanley, 1928, p.25, sketch; one large, two small isles tied on by fringing reef; of typical upper Palaeozoic volcanics, chiefly coarse agglomerates, overlain by basaltic flows, strike N/S, dip steeply W, On W, side is extensive sand flat with recent beach conglomerate a few feet beneath surface. Chart 347.
BARNARD IS, 17° 4 0 !S. 146° 11*E, ? Pre-Cambrian metamorphic rocks and granites* See Egg I*, Jessie I,, Kent I., Rocky I*,
Sisters I, and Stevens I, Chart 2350.
BAYNHAM I . in Cumberland Group, v icin ity 20° 30JS,, Stanley,
1928, p,23, fig , on p.21, appears composed of volcanics. Chart 347.
ELACK I . 200 5 î 53!E. Stanley, 1928, p.14, diagram on po12; low and wooded, extensive fringing reef on E. beach covered with large slabs of recent beach conglomerate containing pebbles o f volcanic rock and rounded fragments o f cora l. Chart 347 =
BORDER I . 200 io ^S. 149° 02*Eo Stanley, 1928, p.10 and drawing, volcanic rocks (?TJpper Palaeozoic) details unknown; some inextensive fringing reefs in the bays. Chart 347o
BCWEN-FROSERPINE CORRIDOR. Stanley, 1928, p035 sketch fig s ,
3 - 22; a llu vial, probably partly flu v ia tile and partly marine; pc47, of rift origin, infilled by combined action of tidal streams and coas bal rivers; full history on p*47.
3REAKSEA SPIT 24 25»S. 153 12»E, Agassiz, 1898, p„90, "a remnant of a former extension of Fraser I.H, criticised by Steers,
1929>P«342, who regards it aj a normal sand spit; "the lightship once 68
drifted hence to Heron I . (Capricorn Group). Henderson, 1931,
p#45j m%p. giving position o f supposed westward migration o f 100
fathom lin e just N. o f th is. Bryan, 1936, p*45> considered
migrations insufficiently supported by evidence. Fairbridge, 1950,
p. 365, consists of dead coral and sand at depth of 1-3 fathoms.
Chart 345«
C. BOWLING GREEN. 19° 20*S. Jukes, 1847, p.55, i t and land
around i t absolutely fla t , o f mangrove swamps and mud fla t s . Steers,
1929* P*343, a long, low, quite typical sand spit formed o f ridges;
at distal end are several recurved ridges; material supplied by
Burdekin R. Chart 348.
C. CAPRICORN. 23° 29 ! S. Fairbridge, 1950, p.368, p rofile
through sh elf. Chart 345»
C. CLEVELAND. 19° 11*S. Jukes, 1847, p.56, granite texÇ -fig.
of granite dyke in granite. Jardine, 1928, p.76; photo. pl.1,fig.3
pi. 2, fig. 2; text-fig. 4. S. and S.E. hills of a coarse grained
biotite-homblende granite in places porphyritic, with aplite
veins and dykes striking E.30° N. and N/S in v ertica l join t planes;
the S.W. hill is of a pale gneissic granite; 1 mile S. of lighthouse,
is a medium-grained acid granite, intruding, in a series o f broad
dykes, thick beds o f banded quartzites which strike W. 15° S. and dip
S.E. 55°> with joint planes N. 20° W., dip S.W. The quartzites,
coarse and fine, alternate with occasional bands of sheared quartz
conglomerate; towards the N. boundary o f the sediments the strike
is W* 10° N o , dip SW 35°j half a mile S. of lighthouse, quartzites
are succeeded by homfels and conglomerate. Jack regarded these
as Upper Bowen (Permian). Jack & Etheridge, 1892, upper Bowen
Volcanics, ashes and lava beds, form Co Cleveland in the eastern 69. extremity of Cleveland Bay, and are like those of Stewarts
Ck. Aus* Pilot IV, p.182, view* Chart 348.
C. CLINTON. 22° 32*S. Jukes, 1847, p.23, porphyry, generally red outside and greyish internally. Chart 346.
C. GLOUCESTER. 200 04«s, Stanley, 1928, p.30, 31, sketch; a residual granite mass,, like that of Ben Lomond to S, where oolitic ? Carb. limestone is intruded; limestone strikes N.W.-S.E. and dips 70° N.E. according to St. Snith, 1918, p«559, but Stanley says it strikes N. 30°E. and dips N.W. very steeply, associated with and overlain by tuffs, lavas and conglomerates. Chart 348.
C. GRAFTON. 16° 52 lS. Jardine, 1925, photo, granite. Aus.
Pilot IV, p. 215, v i e w . Chart 2350.
C. HILLSBOROUGH. 20° 54 :S. Jukes, 1847, p.45. U.Q. Science
Students* Association, Tertiary acid volcanics. Chart 347.
C. PALLARENDA. 19° 11!S. Jack & Etheridge, 1892, p.173, of volcanic ashes and lava beds similar to those of Stewart Js Ck. and
C. Cleveland (Permian). Chart 348.
C. PALMERSTON. 21° 32* S. Juices, 1847, p.39* red quartzose
rocks; two shoal bays above this were rough slate and greywacke or
quartz rock with a dip to the W. in the only spot where stratificat
ion was visible. Chart 346.
C. UPSTART. 19° 42*S. Jukes, 1847. p.52, granite, connected
to mainland by swamps only; p.56, 500 ft. hill on other end of bay granite also. Stanley, 1928, p«42, a granite mass. Steers,
1929, Photo 12. Marshall, Richards & Walkom, 1925, p.29, quote
Stokes 11 a raised beach of 12 ft. above high water mark on the W.
side of C. Up start•” View B on Chart 348.
CID I. 20° 15*S. 148 55*E. Stanley, 1928, p.18, fine-grained 70 and finely stratified (Upper Palaeozoic) tuff, underlain by a massive flow of basalt. Strike N. 20° W, dip S.W. 4-0°; basalt is vesicular in places; no fringing reefs of any extent, probably too steep. Chart 347.
C0GKERM0UTH I . 20° 4 6 TS. 149° 24’E. Steers, 1937, map.p .17. rhyolitic rocks showing benching, higher platform developed, not more than 11 feet above L.W.M. Steers, 1938, p.80, very good map; rh y o litic agglomerates ?Devonian t u ff. Fairbridge, 1950, p.333, small patches of living fringing reef. Chart 347.
C0MPIGNE I . (Port C urtis). 23° 47*S. 151° 16*E. B all, 1904, p.47, E. side, numerous half inch veinlets of very good MhQ2 ore, but nothing workable. (Brisbane metamorphics, D.H.). Aust.l64*
C0MSTQN I . in Cumberland Group, v icin ity 20° 30!S. Stanley,
1928, p.2, f^g. on p.21, p.23, granite. Chart 347.
COOPER PT. 17° 24!S. Jones & Jones, 1956, ?Pre-Cambrian
Barnard metamorphics. View. Aust. Pilot IV, p.214. Chart 2350.
CUMBERLAND GROUP v icin ity 20° 30! S. Stanley, 1928, mainly volcanics (Upper Palaeozoic) and granites. See also Baynham,
Comston, Keyser, Maher, Mansell Islands, Pine Is le t, Thomas and
Triangle Is . Juices, 184-7, p.45 ’’L ittle Cumberland I . is o f rock looking as if made up of angular fragments of compact felspar cemented together.” Chart 347.
CURTIS I. 23° 4 0 ?S. 151° 14!E. Jardine, 1925, p.80 diagram; p.81, flu vio marine plains in north now 15 to 30 f t . above H.W.M.
N. hills of slates, quartzites and sandstones, dip E.300, manganese bearing at C. Keppel. In S, according to Stutchbury, schists and
¿asperoid slates, strike N.E, dip S.W. (Brisbane metamorphics, D.H.)
Aus. 164o 71
DELORAINE I. 20° 10*S. 149° 04 *E. Stanley, 1928, p*8, sketch: pinkish rocks ’’undoubtedly agglomerates" (Upper Palaeozoic.)
Chart 347.
DENT I. 20° 21 !S. 148° 56’E* Stanley, 1928, p.18, figure on p. 19, coarse (Upper Palaeozoic) agglomerates, strike N. 10° W, dip steeply W., simulating weathering of granite, fringing reefs on
N. & E. only* Chart 347*
DOUBLE CONE I. 20° 6*S. 148° 43*E. Stanley, 1928, p.27, of coarse (Upper Palaeozoic) agglomerates and basalts, strike N. 10° W* dip steep E, in places with acid dyking two islands tied by fringing reef. Chart 347.
DOUBLE I, 16°44*S. 145° 40*E. Steers, 1937, p.17, bench awash at high water in steeply dipping phyllites; a small fringing reef. Chart 2924.
DUMBELL I. 20° 11’ S. 149° 01 *E. Stanley, 1928, p.11, details unknown but "certainly composed of volcanics, probably coarse elastics and lavas": a small wave-cut notch around its margin now 4 ft* abo ver high tide. Chart 348.
DUNK I. 17° 55’S. 146° 10’E* Rattray, 1869, p.298, granitic;
Steers, 1929, p.244 Photo. uncliffed* Jones & Jones, 1956, Pre-
Cambrian Barnard matamorphics; Richards’ field notes give strike N.N*W.
dip steep E.N.E.; Richards also notes granite on E* side of island*
Chart 2349*
EDWARD I. 20° 15*S. 149° 11*E. Stanley, 1928, p*9, sketch:
(Upper Palaeozoic) volcanic rocks, breccias and basaltic lavas, strike
N. 20° W, and dip very steeply E; well developed vertical joints N.50°W* on W. or more sheltered side, bench just covers at high water*
Chart 347. 7 2 . EGG I. in N. Barnard Is* vicinity 17° 40 lS. 146° 11?E*, Hedley, 1925, p .6 l, photos, p is . 8-10; Jones & Jones, 1956, of
Pre-Cambrian Barnard metamorphics* Chart 2350.
ESHELBT I. 200 2*S. 149° 37TE* Aust. Pilot 17, p.l63, view:
Stanley, 1928, p.24j low and rocky, of pink granite, cliffed*
Chart 347. FACING I. 23° 53*8. 151° 23 *E. Jardine, 1925, p.83, On N.W. and E. slate s and sch ists (of Brisbane metamorphics) strike N.15° W. dip W. Gatcombe Hd*, of ( ?Pre-Cambrian) sch ists, much contorted, strike N*15° E, traversed by dykes of granite (Stutchbury, 1855),
Aus. 164 * FAMILY GROUP. 18° 03 TS. 146° 13*E. Rattray, 1869, p.298, granitic. Steers, 1929, p.215, Photo 3, granitic. Jones & Jones, 1956, say Hudson I. and probably all the Family Group, are of
Barnard ? Pre-Cambrian metamorphics. Chart 2349* FANTOME I . 18° 41 *S. 146° 32'E.
FITZROY I. 16° 56*S. 145° 59!E. Aust. Pilot 17, p.215, view.
Agassiz, 1898, photo p i. 20; granitic rocks. Steers, 1937, p.21, good example of raised beach at 19 f t . above low water springs.
Fairbridge, 1950, p.333, small fringing reefs. Chart 2350.
FUT TOP I. 21° 101S. 149° 15*E. Marshall, Richards & Walkom,
1925; p»31, dark-bluish-grey f e ls it ic dykes (in ? granite) as at
Townsville and Gloucester I . Chart 347.
FLYING FISH PT. 17° 30 !S. Jones & Jones, 1956. Pre-Cambrian
Barnard metamorphics. Chart 2350. 73
FRAHKUHD Is. 17° U'S. 14.6° 06'E. Rattray, 1869, p.29S, gneissic; Agassiz, 1898, p.110, metamorphic; Eedley, 1925, photo pi» ix-x. Steers, 1929, p«351, partly gneissose. Fairbridge,
1950, p „333, small fringing reef. Jones & Jones, 1956, Pre-Cambrian
Barnard metamorphicso Chart 2350.
GEORGS PT, 20° 04*s. Stanley, 1928, p.32, sketch on p. 24, granitic headland. Chart 348»
GLOUCESTER I. and PASSAGE ISIET. 20° S. 148° 28‘S. Marshall,
Richards & LTalkom, 1925, p.31, dark-bluish grey felsitic dykes similar to those at Flat Top and Holbourne Is. Stanley, 1928, p.30 , of granite; says granites and volcanics of the coastal island are "undoubtedly'5 members of the same suites as the volcanics of the coastal ranges, which he believes Lower Bowen.
Chart 348.
GRASSÏ L 0 20° 8 ‘S. 348° 35* E. Stanley, 1928, p.27, rock appears to be volcanic; slight elevation evidenced by notching and benching. Chart 347.
GR BIST ON PT. 20° 10« S. Steers, 1937, p.18, bench awash
at high water on both sides. Chart 347.
GUM3RELL I.9 20° 6 ! S. 148° 35* E e Stanley, 1928, p.25,
sketch. p Fringing reef on So Chart 347. HAMILTON I. 20° 21 ‘S. B48° 58’S. Stanley, 1928, p.19; geology unknown, probably volcanic, fringing reefs well developed in embaymentso Chart 347. HAROLD I. 20° 15*S. 149° 09!E. Stanley, 1928, p„9, sketch dark coloured volcanics (Upper Palaeozoic); distinct bench just below high water mark; no fringing reefs. Chart 347. 74 HASLEWOOD I, 20° 17* S. 149° 5*E. Stanley, 1928, p.10, tuffs sind agglomerates (Upper Palaeozoic) strike N. 30 E, dip very steeply S,E$ fringing reef extensively developed, and Lupton I . tied to it by a reef. Chart 347, RAIMAN I. 20° 4'S. 148° 54*E. Stanley, 1928, p.11-12, sketch on p,12$ a fairly homogeneous pink granite intersected by small basic dykes, particularly on E, of island! an extensive fringing reef on W. and S, sides, joining Haymanl. to Arkhurst 1 1 no sign of recent uplift, Chsirt 347, HIGH I., 17° 10* s. 146° 01*E, Jones & Jones, 1956. Barnard metamorphics of Pre-Cambrian age, include a biotite kyanite gneiss. Chart 2350. HILDA HILL. 17° 36’S. Jones & Jones, 1956, Pre-Cambrian Barnard metamorphics. Chart 235°. HINCHINEROOK I, 18° 28*S. U6 ° 15'E. Aust. Pilot IV, p.198, view. Richards & Eedley, 1925, p.25, criticism of section through (George*s Pt.) in direction 72° 32*E. by Vaughan, 1917, p,230. Steers, 1929, p.245, the larger, southern half apparently largely of granitei the unnamed cape (a small tied island on the E. side of Missionary Bay mainly of gneissose rock.) Steers, 1930, p.9. Fairbridge, 1950, p.363, refers to large scale cross section of shelf between this and Myrmidon Reef by Richards & Hedley, 1925, p.l. Chart 2349. HOOK I. 20° 6'S. 148° 55'E. Stanley, 1928, p.14, diagram on p,15j incipient dipping! entirely of (Upper Palaeozoic) volcanic rocks, agglomerates and lavas, at least on E. and W. sides, and Stonehaven on W. side, where they strike N. 15° W, and dip W. 40° - o 60 . Rocky Dip is of massive, coarse agglomerates! fringing reef irregularly developed, absent facing deep water but always present 75 in bays» Chart 347. EOLBOURNE I» 19° 44*8. 148° 21,E. Marshall, Richards & Walkom, 1925j p.29 quote St. Smith, 1919. "Whole of E, half of granite, 364 ft* up. The lowlying S,W. section of the island, and a small patch on the N. is of more or less phosphatised coral rock, usually overlain by 2 ft. of soil. Average thickness of phosphate rock, 9 - 10 ft, A raised beach of 4 - 5 ft. is indicated. An elevated fringing reef now dead." Photos. PI,. 3? granite is fine to medium grained, light pink to grey, with fine grained dark bluish grey felsitic dykes like those of Flat Top I, Gloucester I and Townsville, Rainford, 1925, p.l6l, says now dead fringing reef was killed by 1918 cyclones and is not evidence of elevation^ Stanley, 1928, p.24, says must accept this. Steers, 1937, p.18, says perhaps the reef had been uplifted to a critical height before the storm* photo. Fairbridge, 1950 p.333, a shingle bank separating living reef from inner slightly elevated dead reef. Chart 348. HOTTER I, (Duke Group). 21° 58'S. 149° 9'E. Ball, 1904, p, 19, map; N. island highly altered diorite, green tuffy slates, marble and limestone; strike N.N.E. (Devonian) 2 photos; Ball says Jack (1892) on a hurried visit mapped part of the island as granite, but Ball believes this to be simply a highly altered sedimentary rock. Steers, 1937, photo of upper and lower bench. Steers, 1938, p. 67, section through sands and beach. Stubbings, 1938, p.98, foraminiferal sand. Chart 346. IREBÏ I. 20° 14 !S. 149° 9 ’E. Stanley, 1928, p.9. dark coloured rock, and undoubtedly volcanic$ sketch. Chart 348. 76 IEOH X. (Dulco Group). 21° 59’S. 150° 9'E. Ball, 1904, p,9* map and 4 photos ? sla te s and limestones ( ? Lower Devonian) intruded by trachytej haematite and magnetite replacing slate and limestone5 some white crystallin e marble present. Chart 346. JESSIE I. and KENT I. (N. Barnard Group). 17° 40'S. 346° ll'E . Kedley, 192$, p.6l, photos; schist. Jones & Jones, 1956, of Pre- Cambrian Barnard metamorphics, KENT L. with a ta lc antigorite carbonate rock, altered serpentine. KEPPEL BAÏ, ISLkNDS OF. (23°to 23° 31'S). (Brisbane metamorphics). Jardine, 1925, p.84. KEPPEL Rocks, quartzites and contorted shales, strike N. 10° W, dip steep W. with veins of turquoise. ARCH Rock, PEAK I . , SPLIT ROCK, DIVIDED I . , a ll quartzites, shales or schists, dip steep E. S. KEPPEL I. (GREAT KEPPEL I.) on the N.W., quartzites and shales strike W, 22° N, dip S.W, 25° (Photo in Steers, 1937, bench in contorted rocks) N. KEPPEL I. gently dipping snadstones, quartzites, mudstones and phyllitic rocks; on E, side of island, sandstones strike E - IJ, and dip N. at 1$° - 20°; on N.E. side, strike W. 30° N., dip U.E, at 15°; photo 2 0 ;*! (Jack & Etheridge 1892 describe these rocks p*91 as slates and greywackes dipping at high angles to the N,Vi and intersected by dolerite dykes). MIDDIE and MYALL IS., quart zite s* BLUFF ROCK, CREEK ROCK, DOUBLE HEAD and BLUFF PT., trachyte plugs Tertiary. Chart 345. KEYSER I. in Cumberland Group, vicin ity 20° 30'S. Stanley, 1928, fig, p.21; p.23, pink granite. Chart 347 UHGFORD I , 20° $*S. U B ° 52’E. Agassiz, 1898, photo Stanley, 1928, p.13, sketch p,12; appears to be formed of volcanic rocks. Chart 348. 77. LINDEMAN I. 20° 26'S, 149° 3 ,E. Lenox-Conyngham & Potts, 1925, photo; Aust, Pilot IV, p.142, view. Stanley, 1928, p.19? elastics and lavas of the (Upper Palaeozoic) volcanic series, strike N.N.W. - S.S.E., dip 45° E.N.E., basaltic rather than andesitic (ferro-magnesian free). Chart 347. LINDQUIST I. 17° 39'S. 1A6° 06»E. Steers, 1937, p.23, traces of a higher bench 22 ft. above H.W.M, east in schistose rock. Jones & Jones, 1956, Pre-Cambrian Barnard metamorphics. Chart 2350. LONG I. Broad Sound. 22° 10'S. 149° 53'E. Aust. Pilot IV, p.101, ’porphyry'. Ball, 1904, p.12 "iron ore deposit reported". Chart 346. MACKENZIE I. in Fitzroy R, estuary. Jardine, 1925, p.116, a fluvio-marine monad no ok of what is probably horizontal upper Cretaceous sandstone occurs on it , with marine cliffs and benching round it 100 yards from shore line or 15 to 20 ft. above present E.W.M. i a low proportion of rhyolitic rock at upstream point of island. MAGNETIC I. 19° 9'S. 146° 50'E. Aust. Pilot IV, p.183, view. Maitland, 1892, geological map; Jack & Etheridge, 1892, p.173, volcanic ashes and lavas at W. corner are similar to the U, Bowen of Stewart's Ck., Townsville j remainder of island granite, thin section described on pZLO as obviously belonging to the same series as one from Kipper Pt., Mt. Elliott, near Townsville. Jardine» 1928, p.78, granitic. Fairbridge, 1950, p.333> good fringing reef on S.W. Chart 2349. MAHER and MANSELL IS. (Cumberland Group), vicinity 20° 30'S. Stanley, 1928, fig, on p.21| p.235 MAHER I. volcanic but details unkowni MANSELL I. same pink granite as SHAW and other islands thereabouts, Chart 3£7. 78, MARBLE and MORTAR I . (Duke Group). 22° S. 150° 11*2* B all, I 904, p.19, map; photos; greenish schistose tuff slate, clay slate and limestone of Devonian age. Jack mapped part as granite, but Ball says this was merely interstratified crinoidal limestone. Steers, 1937, p.22, an old c l i f f lin e , now untouched by waves, hear Lola Montez Pass. Chart 346, MAUSOLEUM i. 20° 52'S. 148° 56’E. U. Dev, or L. Carbi sediments and volcanics, with ? Jurassic sandstones Chart 347. MIDDIE I, Edgecumbe Bay, 19° 59'S. 148° 22'E, Agassiz, 1898, photos pis. 1-4. Stanley, 1928, p,36 sketdh on p¿37; granite; says Agassiz 'elevated reef* is only beach conglomerate on a bench 12 - 15 f t . wide and 5 f t . above H.W.M., but is unr- doubted evidence of elevation. Steers, 1929, p.346, photo discusses Agassiz remarks. Chart 348. MOT JE IS, 20° 15'S, 148° 50'E. Jukes, 1847, p.47; hard to say whether igneous or metamorphic rocks. Stanley, 1928, pi27, sketch, p*26i Volcanic series (Upper Palaeozoic) strike N*20°W., dip N¿E. 60° - 70°é Lowest rocks basaltic lavas, overlain by agglomerates, followed by a coatfso grained dolerite* followed by hard, dark black, fine-grained cherty rocks (resembling tfadiolar- ian cherts) intercalated with thinly bedded lavas and tuffs. Cherts probably tuffaceous in origin, no radiolaria seen in thin section. Chart 348. MULCRAVE CORRIDOR. Jardine, 1925, p.133, wclearly a small rift valley; the Barron, Mulgrave, Russell and Johnstone in their present form postulate tho foundering of the eastern continental margin; alluvial deposits on floor about 4 miles broad; alluvium terraced, one at 75 f t . above river at Walsh's pyramid, photo p i. 25, one at 30 f t . (3/4 mile wide) narrowing southwards1'. 79 NEWRY I. (Outer and Inner). 20° 51*S. 148° 56*E. U. Dev, or L. Carb. sediments and volcanics, with ? Jurassic sandstone. Chart 347. N0RMANBY I. (Frankland Is.). 17° 13‘S. 046° Q4'E. Jones & Jones, 1956, Pre-Cambrian Barnard Metamorphics. Chart 2350. OLDEN I. 20° 6'S. 148° 34’E. Stanley, 1928, p.25, of dark coloured rocks almost certainly volcanic; slight uplift indicated. Chart 348. PAIM IS. 18° 44!S. 146° 36'E. Jack & Etheridge, 1892, p.719, describe thin section of a basalt; AgasSia, 1898, Photo«, pli 19; Andrews,1902, p¿Í46; Saville Kent, 1893> Photos of ireef (very extensive fringing reefs, inner parts sediment-covered). Fairbridge, 1950, p.333. Richards, 1923, M.S., pink granite. PERCY IS. 21° 41*S. 150° 14'E. view. Lust. Pilot IV, p.114. Chart 346. Richards, 1936, M.S., rhyolites, etc., dip 45° PINE ISIET, Cumberland Group, 20° 31*S. 149° 06*E. Stanley, 1928, p.21, figure, p.23, pink granite. Chart 347. PORT CURTIS ISLANDS OF. See CCKPIGNE, PICNIC, QUOIN, TIDE and TURTLE IS. Jardine, 1925, p.83, of sandstones, quartzites and schists, frequently the latter, and intensely crumpled and intruded by quartz stringers (Brisbane Metamorphics). Chart Aus* 164. POOLS and THOMAS IS. (Edgecumbe Bay). 20° 5'S. 148° 19*E. Stanley, 1928, p.38, wPoole reported basaltic“. Stanley presumes these to be, like the volcanics of Ben Lomond, Permo-Carb, Chart 348. PICNIC I. (Pt. Curtis). 23° 4.9'S. 151° 14'E. Ball, 1904, p.36. 47; dyke of sanidine trachyte in Devonian slates and trachytes at S. end of island numerous veinlets of good Mn ore, but nothing workable. Aus. 1 6 4 . 80 QUOIN I. (W. of Facing I.) 23° 49‘S. 131° 17^. Ball, 1904, map, turquoise veinlets shown at S. end. (Thin bedded quartzites, Brisbane metamorphics). Chart Aus. 164. RATTRAY I. 20° 0'S. 14.8° 33'E. View, Aus. Pilot IV, p.163. Stanley, 1928, p.24, of volcanic rock, details unknown. Chart 348 o 0 REDCL1FF Is. (outer and inner). 20 52‘S. 148 58'E. U. Dev. or L. Carb. sediments and volcantes. Chart 347. ROCKY I. (N, Barnard Is.). 17° 40'S. 146° ll'E. Jones & Jones 1956, Pre-Cambrian Barnard metamorphics. Chart 2350. ROCKY PT. 17° 22*S. Jones & Jones, 1956, Pre-Cambrian Barnard metamorphics. Chart 2350, RODD’S PENINSULA. 24° O'S. Vaughan, 1917, p.230, profile N. 50° E. through Fitzroy Reef. See Richards & Hedley, 1929, p.25, for criticism. Chart 345. RUSSELL I. (Frankland Is.) 17° I4'S. 146° 06«E. Jones & Jones, 1956, Pre-Cambrian Barnard metamorphics; includes andalusite- cordierite gneiss; Hedley, 1925, p.62 photo. pis. 9, 10; Steers, 1929 , p.351, partly gneissic. Chart 2350. SADDLEBACK I. 20° 4'S. 148° 32'E. View Aust. Pilot IV, p.163. Stanley, 1928, p.24, sketch; of pink granite, strongly N/S jointed, either vertical or steep E; basic dykes common; cliffed on E,; granite closely resembles that of Gumbreil I. Chart 348. SCAWFELL I. 20° 32*S 14-9° 37'E. Richards, MS., pink granite. SEAFQRTH I. 20° 28!S 149° 02*E. Stanley, 1928, p.20, sketch on p.21; pink granite, cliffed. Chart 347. SHAW I. 20° 30!S. 149° 05'E. (with nearby BRUSH I. and YELLOW ROCK), Stanley, 1928, p.20, fig, on p.21, south of Neck Bay is entirely granite (pink, like YELLOW ROCK with slightly opales cent quartz) strongly jointed, strongest joints being N. 60° E. dip 0 50 S, and intruded by numerous small dykes. A sandy isthmus m Neck Bay conceals junction of granite with the (Upper Palaeozoic) volcanic tuffs, agglomerates and intercalated andesites and basaltic 81. lavas of the H. part, which strike S. 80° W. and dip steeply H, o o at 60 - 75 , and are chocolate in colour. Brush I. is of granite with a basic dyke. Chart 347. SISTERS AND STEPHENS IS. (S-. Barnards) 17° 44*S. 146° 10»E Andrews, 1902, basalt (recent) dykes occur on Stephens I. Steers, 1929, Stephens I. of volcanic tuff. Jones & Jones, 1956, both of Pre-Cambrian Barnard met amor phics. Chart 2350. SNkPEERI. 16° 17'S. 145° 30'E. Fairbridge, 1950, p.335, fringing reef. Chart 2924„ STAÎÏNAGE FT, 22° 9*S. 150° 2»E. approx. Ball, 19C4, p.12, man; Iron Knob is on E. side of Stannage Pt., and is a ? meta- somatic deposit of greenish 'Euffy slate and conglomerate, clay slate and limestone (now marble or ore) magnetite and haematite. Chart 346. STONE I. (Pt. Denison). 20° 02'S, 148° 17*E. Hedley, 1925, p.35, flourishing fringing reef destroyed by rainstorm in 1918 hurricane (19 inches in 3 days) coinciding with low spring tides. Stanley, 1928, p.37, felsites and porphyries intruded in places by dykes of underlying granite. Steers, 1937, p.lB, photo. Steers, 1938, p.80, map. Fairbridge, 1950, p.333» Chart 348. TAM 0»SHATTER FT. 17° 58’S. Jones & Jones, 1956, Pre- Cambrian Barnard metamorphics. Chart 2349. THOMAS I. and TRIANGIE I. Cumberland Group. vicinity 20° 30*S. Stanley, 1928, fig. on p.21, p.23 granite. Chart 347. TIDE I. 23° 48* S. 151° 15'E, over folded thin bedded quartz ites, Brisbane metamorphics. Aus. 16 4 . T GRILLA MARINE PLAIN. Jardine, 1928, p. 88, photo. pi, 4, 5, slope gradually from sea level to 100 ft,$ mostly under 40 ft$ marine shales scattered on surface. 82. TREBIE I. (Guardfish Cluster). 21° 35'S. 149° 46'E. Steers, 1937, p.18, photo. a complex structure including volcanic agglomerates intersected by dykes. Chart 347. TURTLE I. (Pt. Curtis). 23° 4 8 ’S. 151° 15'E. Ball, 1904, p.47, map; a manganese quarry has been opened on a band of slate 10 ft. with and partly replaced by Mn and quartz. Strike approx. N.N.W. vertical. (Brisbane metamorphics.) Aus. 164. UPPER HD. (Broad Sound). 22° 10*S. Aus. Pilot IV, p.101. stone of this and apparently of all the hills in its neighbourhood is granitici while that of Long I. and West Kill approach nearer to porphyry. Chart 347. WALSH’S PYRAMID. Gordonvale, N.Q. Jardine, 1925, p.129, recent beds (Lacustrine) 100 ft. above sea level fringe Walsh’s Pyramid and have not been elevated. WEDôE I. 20° 55'S. 149° 4 ’E. Tertiary volcanics with some sahdstone with fossil dicotyledonous leaves interbedded. Chart 347. WEST HILL (Broad Sound). 21° 50’S. Jukes, 1847, p.31> a very fine grained tuff or basalt, with small crystals of felspar only visible with a lens. The rock is split by innumerable veins and joints.. , Chart 347. WHITSUNDAY I. 20° 10’S. - 20° 20'S. Saville Kent, 1893, photos ; Agassiz, 1898; Stanley, 1928, p.16, map and figs 10-12; as fer as known, only (Upper Palaeozoic) volcanic rocks, agglomer ates, layas and tuffs, examined at Hill Inlet in S.W.; here strike o o N.5 W; at E. end of section dip 65 W.; further W. dip lessens to o 20 ; agglomerates with interbedded trachy-andesitic flow, Whitsun day Peak is of volcanics, strike N.15° W, dip steeply W, an anti cline limb, see fig. 24. A bench‘4 ft. above High Tide. Steers, 1929, P.247. The steep limb of the Whitsunday fold faces E, W*H. Bryan has drawn an important anticlinal axis of the closing Mesozoic folding here. Chart 348. A.II.g. BORDES THROUGH CAYS ON MICHAELMAS KBEF AND. HERON i". These are the only two bores into the reef. Michaelmas Cay lies in 16° 36'S. H 5 ° 58'E. and Heron I. in 23° 26'S. I5I0 57'E. The following summary of results is extracted from pp.106-7 of RICHARDS, H . C . and HILL, D., 1942, Great Barrier Reef Bores, 1926 and 1937 - Descriptions, analyses and interpretations - Rept. Great Barrier Reef Committee, Vol. V, pp. 1-122, which work, with Plates IX and X giving tabular representations of the borings, is included as an Appendix to this present report: "Finally it is clear that those characters common to both bores must be those which are of importance in a discussion of the formation of the Great Barrier Reef. These are (1) the great thickness of reef materials in the upper part of each bore - 506 feet at Heron Island and 37Ö feet at Michaelmas Cay (2) the occur rence of reef corals through the top 506 feet of the Heron Island bore and the top 476 feet of the Michaelmas Cay bore (3) the occur rence of quartz-foraminiferal sands below the reef rock, to a depth of 732 feet at Heron Island, and 600 feet at Michaelmas Cay (4) the absence of a basement even at 732 feet. That similar conditions have affected the materials since their deposition is shown by (5) the absence of dolomitisation, (6) the presence of two aragonite zones and (7) the lack of sufficient cohesion in the material to yield cores comparable with those obtained at Funafuti and the Bahamas, We conclude that conditions must have been favourable for the luxuriant growth of reef-forming corals and associated forms of life along the Great Barrier Reef region during the time represented by the deposition of the 506 feet of reef materials at Heron 84* Island. Twenty five (or at the very greatest thirty) fathoms is the depth now generally accepted as the maximum at which reef corals may flourish so well as to form a reef¿ though this maximum is thought by some to decrease with distance from the equator. Some authorities consider that 5 or 6 fathoms is the depth of most luxuriant coral growth, but all agree that at a depth below 30 fathoms only occasional coralla occur. We think it is clear then, that at least 320 feet or rather more than 50 fathoms of subsidence must have occurred during the period represented by the reef rock. The mollusca of the Heron Island bore indicate that here the sands and hard bands below the reef rock are also shallow water deposits; so that about 40 fathoms further subsidence is probable for this region. We have no study of the mollusca of the Michael mas Cay bore but the similarities between the two bores are such that it is reasonable to assume an identity of history. Since all of the mollusca and corals throughout the Heron Island bore are found living in the same region today there must have been little or no variation in the climatic conditions of the area; i.e. the deposits show no sign of the Pleistocene ice age and are clearly later than this. The occurrence of none but recent species of corals and molluscs indicates that the bores passed through materials deposited entirely during recent times, so that the subsidence of about 100 fathoms and the deposition must have been rapid*’. 85 •B. THE GEOLOGY (OR GEOMORPHOLOGY) OF AREAS ADJACENT TO THE CONTINENTAL SHELF OF QUEENSLAMD-PAPUA Having surveyed what is known of the shelf itself, we may now proceed to examine what is known or thought about neighbouring areas, for the sake of any help such might give in deducing what lies under the shelf* 86 B.III. THE GEOLOGY OF EASTERN NEW GUINEA This is considered insofar as it may be relative to the geology of the Reef area between Bramble Cay and Trinity Opening. Glaessner (1950) took account of all known geology of New Guinea in formulating the scheme of geotectonic elements that may fomthe beginning point for our discussion. These are illustrated in the accompanying fig. That part of Papua that is nearest to Queensland, at the Torres Straits, he regards as part of the stable or cratonic region of Australia,' and in this we may follow him. Only 60 ft, of water today covers the sea floor in the straits and eastward to the edge of the Barrier at Bramble Cay; all the high islands west of 14-° are of granites, pyroclastic or metamorphic rocks quite similar to those of the northern end of C, York Peninsula; there seems no reason at all to doubt that the Pre-Cambrian and. Palaeozoic features of the Peninsula continue northwards across the Straits and into Western Papua (Mabaduan Hill) as submerged mountains whose tops only are visible today as high islands. The Oriomo R. bore at Maremosab bottomed on biotite granite identical in all respects with that at Mabaduan Hill. How far north does this ’Australian’ basement extend? In Glaessner’s view, with which I agree, it continued to but is in creasingly less stable towards the foothills and the highlands that run E.S.E. and tS.E, through New Guinea. These highlands he regards as formed from a géosynclinal region of maximum mobility that dates back at least into the Permian, circumferential to the Australian continent. Montgomery, Osborne & Glaessner (1944- p*22) expressed the views that the crystalline rocks of Figure r-f ter G 1 " essner, showing " truc t nr ? 1 I emente. 1. °outhern tat le Area 2. Fly-Vipoel 'half 3. Fo’ded sedimentary zone A-. Crystal1 23*7891011 ine zone G. Northern geos ne'ine G. G-cl os Mts, metamornhics 7. Volcanic Arc of Bismarck • ea 8. )Vogelkot> bas:n and surrounding mountain arcs 9. ) 10, Aure Trough 11, Marche arc and Owen Atante'r folded zone 10, Fini-ter■e Mountains S7 the Central Highlands arc essentially great linear basement uplifts on which the folding of the sedimentary cover is a secondary feature, that there is no evidence of the great overthrusts of Alpine type which were previously thought to exist there, and that the mountain building movements were vertical rather than horizontal. Rickwood's (1955) studies in the Central Highlands seem to support this view, though basement and overlying strata appear to have been folded by compression accompanied by a considerable vertical com ponent force, giving markedly asymmetric anticlines with the steeper flank on the south west, with high angle strike ih’-'ust faulting. Deutorically altered doleritic and porphyritic late Miocene intrusives appear related to the faulting, but there are no granitic masses associated with it. From this region of maximum mobility, trans gressive seas spread south and south-west over the more stable region. Glaessner (1950) draws a tentative boundary between the Stable Region and the Region of the Fly-Digoel Depression that has sub sided somewhat more, the boundary running parallel to but a little S. of the Fly R. These two regions are largely covered by the recent alluvia of the Fly-Digoel Rivers. Mio-Pliocene limestones and sediments are probably present throughout both regions, lying unconformably on the granitic or crystalline base ment as at Mabaduan Hill and Oriomo R. The sequence of strata in the Oriomo district is of importance in our consideration of oil potential in the reef area lying between Torres St. and the Murray Is., and the stratigraphic column from the %remosab Bore is given as an appendix to this section. Gray (1928 in A.P.O. reports Vol, II, p,13) considered that the folding (along E.-W Lines) 88 in the Oriomo region was so extremely slight that the structures offered no likelihood of oil doncentrâtion therein; also the structures were filled with water to their caps# Between the Fly-Digoel Depression and the Central Highlands there lies a folded sedimentary zone in the Papuan Basin (Montgomery, Glaessner & Osborne, 1950) where the Mio-Pliocene limestones have been uplifted and folded less gently# These limestones were earlier regarded as Pleistocene# In the Purari watershed, similar but slightly stronger folds expose also Apto-Albian and Cenomanian strata. S t i l l further north in the Wahgi-Chimbu valleys, and in the Mt#Hagen area of the Central Highland (Rickwood, 1955) crystalline basement, Permian marine, followed uneonformably by Upper Jurassic marines and these by Upper Cretaceous, Eocene, Oligocène and Miocene marine, are followed unconformably by Pleistocene terrestrial volcanics. Further west, at the headwaters of the Fly and otrickland Rivers, Middle Ju rassic is known, but neither Permian strata nor the basement was seen (Osborne, 1945)* Thus there is considerable instability evident in the folded belt, and there is much to be said for Glaessner's view that transgresión spread south and south west for greater or lesser distances over the more stable regions. Cloarljr, Miocene strata reached as far as thé Papuan coast S.U. of Mabaduan Hill, but since they lie directly on basement there, i t seems that Mesozoic and Palaeogene transgressions, if any, did not extend that far in that direction# The remaining tectonic elements of Glaessner's scheme that lie to the north of the folded zone are not germane to our present enquiry and may be neglected. 89. However, we need to consider now the south-east part of Papua, that forms the eastern boundary of the northern part of the Coral Sea, Glaessner (1950) has considered the tectonics of this region related to a different control from that of the region already con- sidered. All the Mesozoic and Tertiary sediments we have considered so far are unmetamorphosed. The deep bore at Kariava has proved the existence of a deep trough, the Aure Trough (see Fig, 1) filled during the Miocene with quantities of tuffaceous greywackes (Edwards, 1950a, b,) and this is interpreted by Glaessner (1950) as a great fore-deep to the orogenic region of Morobe, where diastrophism was more intense than in the Central Highlands area, and where the great Morobe batholith (Fisher, 194-4) has caused the cover rocks to be metamorphosed (Kaindi metamorphics)• On the Snake R. these meta- morphics have been shown to include Cretaceous (probably Upper Cretaceous) rocks. In the Morobe area the fold axes run N.E., but Glaessner considers them to swing in their S.W. parts round to the S, and eventually towards the S.E., where they become continuous with those of the Port Moresby District. It would appear that the Kuru boring was put down in a region which the operating company may have interpreted as a hinge area between shelf and mobile basin. In the Port Moresby district (Glaessner, 1952) the folding seems to have been Miocene; basement is not exposed here, the best rocks known being marine Cretaceous (Upper Senonian)• In these Cretaceous rocks Glaessner recognises two facies, the western (Barum sandstone, 100 ft. exposed of bedded calcareous quartz sandstone with orbitoidal forams), which he regards as 90 a noar-shore facies, and the eastern (Bogoru Limestone, 300 ft, observed, pink, dark and generally intensely sheared, with pelagic forams) which he considers further off-shore. From this he deduces that in the late Cretaceous a shore line existed in the Coral Sea, the land to the west of it. Upper Eocene and Oligocène sediments of géosynclinal type characterise the Port Moresby area, and from their facies changes and from derived Eocene fossils in the Oligocène, Glaessner deduces that Eocene shelf limestones were deposited in the Coral Sea area, but were being eroded during the Oligocène, during which time also granitic basement may have been exposed in the Coral Sea to serve as a source for granite debris in the Oligocène sediments. Folding during the Miocene prevented marine sediments from being deposited in the Pt. Moresby area, in great contrast to the deposition on the Oriomo shelf region; instead, synr-orogenic fluviatile sediments were formed, and intrusions of gabbro occurred. Serpentine is known, but is earlier than the main folding, being pre-01igocene, post Eocene. Post-orogenic explosive andesitic vulcanicity produced the Miocene Astrolabe agglomerates and tuffs. Pleistocene coral reefs have not certainly been identified but Sub-recent and Recent coral reefs arc present off the Port Moresby coast of Papua. They are donfined to a narrow belt close inshore, and the seafloor falls away sharply outside the belt, the pattern indicating a plunging youthful coast line and suggesting orogenic activity. This is in sharp contrast to the great width of the shallow platform from which coral reefs arise on the western side of the head of the Coral Sea, where the 91 geomorphology suggests cratonic sta b ility . References to New Guinea Geology used in the above Review. For Titles and Journals see Bibliographic List at the end of Report. Anglo Persian Oil Co., 1930 Australian Oil & Gas Journal Vols. I, II. B eltz, 194-4 Carey, 1945 Edwards, 1950a, 1950b. Edwards & Glaessner, 1953. Fisher, 1944 Glaessner, 1943, 1945, 1949, 1950, 1952. Maitland, 1892, 1905. Montgomery, Osborne & Glaessner, 1944, 1950 Osborne, 1945 Rade, 1953 Rickwood, 1955 Stanley, 1922, 1924 Wilkinson, 1877. 92 APPENDIX I TO THE GEOLOGY OF EASTERN NEW GUINEA Late Tertiary stratigraphical sequence in Oriomo R. areas From W.M. Gray, A-P.O. Vol. II Top* Pliocene Imbi Group, a thin upper group of clays, sands, silty and detrital fossiliferous limestone, 50-100 ft* Miocene Oriomo Limestone. 14-30 ft. thick (measured in Maromosab Bore)* (iii) Coralline Zone. Porous limestone (? possibly reef limestone) containing corals, bryozoa, Lithothamnium. casts of large and small mollusca and Orbitolites 0-700 ft. (ii) Intermediate Zone. Hard blue and grey limestones, with interbedded soft chalk containing an abundance of Polystomella and some bryozoa and Orbitolites (700-900 ft.) Hard blue and grey limestones and chalky limestones Bands rich in M iliolaT Lithothamnium, Polystomella and shell fragments* (900-1,150 ft.) (i) Orbitoidal Zone. Alternating beds of limestone and chalk containing an abundance of Lenidocyclina (1,150-1,4-76 f t.) . Basement, a biotite granite identical in all respects with that from Mabaduan H ill. 93 APPENDIX I I t o the GEOLOGY OF EASTERN NEVI GÜINES. SOUTE OF THE HIGHLANDS Published Information on Bores drilled for Oil (From U. t o E .) . Morehead on Morehoad R., not yet started. Aramia No. 1. (Aust. Oil & Gas Journal, II, No. 4, p.8. Jan. 1956). Total depth, 6628 ft. Completed October, Basement 6530« ft* Qriomo Maremosab, 1475 ft, of Miocene Oriomo Lst. above Basement of biotite granite. Wohomul No, I.- Miocene Oriomo L st. to 1250 f t . Wohomul No. 2.- Miocene Oriomo Lst. to 1475 ft.-, then a rock group composed of crystals of clear quartz and angular quartz grains, with pyrites to 1573 f t i probably weathered basement granite, then very hard rock giving in sludge pump sharp fragments of quartzite with talc and biotite. No. 4 bore in this area mentioned, but ho data found. Omati No. 1, (Aust. Oil & Gas Journal II, No.-4, p.7). Total depth, 14,352 ft. Completed in April 1955* Tops of Formation, Tertiary 10,065 ft# Cretaceous; Petroliferous gas at 13,740 ft. Omati No. 2. Total depth 10,880 ft. Completed July, 1955. Tops of formation, Tertiary, Cretaceous. Bar eke w a.- Just storting. Kuru. Down t o 449 f t , on Jan# 1 s t, 1956. Gas at 998 f t . Kariava. No# 1. Drilled to 12,621 ft. Wana. Drilled to 9,866 ft. This is reported to be the only E. New Guinea well with reservoir-type rocks. ÏÏDoia. Drilled to 5.350. ft Horohoro No. 1 . 4,721 f t . Horohoro No. 2. 10,642 f t . Pono. 5 wells, the deepest 2,707 ft. Oroi. 5,516 ft. Oiana. no informati on Yule I . (on coast N.W. from) 2 bores. The Papuan A p in aipi Concession between the Mouth o f the Purari R* and I 47 E, is said to be still on the shelf region. THE GECrlflGY OF B. IV. CAPE YORK PENINSULA CAPS YORK TO PORT DOUGLAS. 1» Details of and References for Regional Geology4 The Peninsula consists fundamentally of a pre-Mesozoic base ment covered by some 2000 ft. of Mesozoic sandstones and shales, fresh water below and marine above; the whole being capped by thin Tertiary continental deposits and late Tertiary latérites with a few valley basalts in east coastal regions, a. The Basement. The basement is very different on either side of a line, the Tasman Line (Hill, 1951, 1952) through Shelburne Bay ( approx imately 143°E), which as it is followed to the south, swings S.S.E. to follow the main trend of the coast, passing just west of Coen and of Mungana and Chillagoe (State Map, 1953) • West of this line, the basement consists of gneisses, highly micaceous schists, quartzites and phyllites, occurring as islands in a vast sea of granite which normally is a coarse grained biotite granite varying in colour from grey to light pink, with an abnormal development of large felspar crystals; this granite extends southwards from Temple Bay to Princess Charlotte Bay, and thence to the Alice River Goldfield (200 miles Morton, 1924). Similar basement occurs in the vicinity of C*. York and Somerset (Morton, 1924) and rocks similar to those of C. York and Somerset have been recognised by Jukes (1847), Rattray (1869), Haddon, Solías and Cole (1894), Shepherd (1944) and Jones and Jones (1956) in the rocky islands of Torres Straits 95 o north of Papua and\est of 142 50’E. At Cape York and in the Torres Straits islands, the granitos, syenites and metamorphic rocks are intruded by quartz porphyries which may have associated extrusive and pyroclastic quartz porphyries, and whose age is thought, by their similarity to porphyries in the Pascoe River area, to be post-Lower-Carboniferous and pre-Jurassic or pre- Lower Cretaceous* The granites and met amor phics are now generally regarded as Pre-Cambrian, and, while entirely unlikely to contain oil, are good metal prospects, particularly for wolfram, gold and the rare metals. East of the Tasman Line, the basement consists of Palaeozoic rocks* In the extreme S.W., a belt of quartzites and limestones (possibly ancient coral reefs) of Silurian and Lower Devonian age, the Chillagoe Series, lies against the Pre-Cambrian, dipping steeply eastwards, and altered by mineralising granitic in trusions! this belt passes northwards of the Palmer River tinder, the Mesozoic cover (State Map, 1953) but may be represented in the far north at Bolt Head in Temple Bay by a 100 ft. limestone of quasi-schistose structure, dipping 45° E. (Jack, 1922, p*568), where also serpentine outcrops close by. In the extreme S.E., along the coast, a belt of quartzites and slates, the Barron metamorphics, very like the Brisbane metamorphics, has steep dips and is intruded by numerous tin bearing granitic batholiths. It is quite unfossiliferous, though limestone has been reported near Mt. Byerley, S.W. of Cooktown and near Mt. Armit S.W. of Daintree. This belt is either older than or equal in part to the Chillagoe Series. It may be 96 represented, re-emerged to the North from under the Mesozoic cover, by the shales, slates, sandstones, greywackes, tuffs and leucophyres of the Starcke River goldfield described by Ball (1909), or by the silicified slates (Ball, 1910) of Mt. Ruby area, or by the slates in places schistose of the Laura River area (Ball, 1910). Between the Chillagoe Series and the Barron Metamorphics lies the Hodgkinson Series, a very thick (21,000 ft. Jack, in Jack & Etheridge, 1892) group of shales, greywackes, grits and conglomerates, with a few thin limestones, Lepidodendroid remains are known from the greywackes, and corals from the limestones, and an Upper Devonian - Lower Carboniferous age is indicated. The strata dip steeply and are mineralised along the Palmer, north of which they pass under the Mesozoic cover. They are represented much further north, along the Pascoe River, by indurated shales, ferruginous sandstones at times conglomeratic, grits and probab3y also coal seams, since Morton (1924) has found lepidodendroid remains here also. These northern beds are invaded by quartz porphyries which in places are associated with extrusive and pyroclastic quartz porphyries. These post-Lower Carboniferous porphyries of the Pascoe River are in Morton* s (1924) opinion identical with those invading the Pre-Cambrian granites and metamorphics in the vicinity of Cape York, and hence with those of the Torres Strait islands. On the Pascoe they are seen to be overlain by the Mesozoic sandstones, here either Jurassic or Lower Cretaceous. The youngest Palaeozoic sediments of eastern Cape York 97, Peninsula are the Permo-Carboniferous coal measures of the Little River, which are of blue and dark shales, gritty sand stones and fireclays with numerous thick coal seams, highly tilted in a N - S. graben dropped into older rocks* These strata, presumably deposited in a small terrestrial basin, contain Glossonteris * the typical Permo-Carboniferous le a f. Another small patch of similar strata with similar fossils is known on Oakey Creek, W.S.W. of Cooktown, dipping at high angles N.W. beneath the overlying almost horizontal Mesozoic sandstones (Jack, 1922; Jack & Etheridge, 1892, pp. 174* 175). b. Earth Movements and Plutonism affecting the Basement. The Chillagoe Series is unconformable on or faulted against the Pre-Cambrian; an unconformity of the Hodgkinson Series on both Chillagoe and Barron Groups is suspected, since the two la tte r show low grade metamorphism, and the former does not, but i t has not been proved in the fie ld . By analogy with S. Queensland, i t is considered probable that an important orogeny occurred in mid-Devonian times, affecting the Chillagoe and Barron Groups, and providing relatively highlands from which detritus that was to form the Hodgkinson Series was poured into a narrowed but rapidly subsiding basin. The Temple Bay serpentine possibly appeared at this time. Some of the granites invading the two older groups may belong to this orogeny, but again nothing has been proved in the fie ld . The Hodgkinson Series has been folded and intruded by granites in post-Lower Carboniferous, pre-Middle Carboniferous times (on evidence of unconformability of Rhaconteris bearing volcanics and glacials south of the 98 Peninsula in the Silver Valley (Reid, 1930)5 in the Pascoe River area equivalent sediments have been tilted or folded and invaded by quartz porphyries before their ? Jurassic or Lower Cretaceous cover was deposited* The Permo-Carboniferous Coal Measures were tilted and downfaulted before their Mesozoic cover was deposited* c* Maior Structural Units of the Basements. Prom the details given above, it may be deduced; i, That the area west of the Tasman Line is part of the stable Pre-Cambrian Shield* ii. That the area oast of the Tasman Line was part of the mobile Tasman geosynclino, and was (1) depressed during Silurian and early Devonian times in relation to the Shield to the westj receiving much sediment; and was (2) folded along N.N,W* or meridional lines, possibly with serpentine intrusion during mid-Devonian, and probably also with granitic intrusions* (3) depressed again in a central N.N.W. belt during late Devonian or early Carboniferous times, with formation of the Hodgkinson Basin (Hill, 1950), which received huge amounts of sediment, iii. That the Hodgkinson Basin sediments were folded immediately before Middle Carboniferous times, probably with granitic intrusion, and emergence. iv. That the whole of this Peninsula part of the Tasman gcosyncline was thereby so stabilised that it reacted after Middle Carboniferous times as if it had been welded on to and become part of the Shield. V. That Permo-Carboniferous coal measures formed in small basins on the newly emergent land, d. Mesozoic Geology and the Surface of the nre-Mesozoic Basement. The Mesozoic rocks are sandstones and shales with some conglomerates, mainly freshwater; marine strata are confined to the Aptian Stage of the Cretaceous period. No interbedded 99 volcanics have been reported and no plutonio intrusions are known. Jack (1881, and 1922 p.516) seems to have thought that granite near Battle Camp was younger than the Mesozoic sediments there, but B all (1910) mapped the junction as unconformable, not intrusive. Dips are very slight (except near the faults bounding the L ittle R. Permo-Carboniferous Coal Measures) in general not greater than 1 in 100 or 1 in 200 (Ball, 1909, 1910)• Mesozoic strata outcrop in two separate regions related to the present Main Divide (State Map, 1953)• i . The Laura Basin (H ill, 1951, 1952) lie s between Princess Charlotte Bay and the Main Divide. Its strata fall at a very slig h t dip inward from the Coastal Ranges (Jack, 1881j Jackson 1902j Ball, 1909,1910), but their attitude on its western margin in unrecorded. Denmead (oral communication) informs me that they dip steeply in the vicinity of the faults bounding the Little River Permo-Carboniferous coal measures; Jack (I8SI) rogarded them as abutting against both the Coastal ranges and the Main Divides, which he pictured as forming the shorelines of a depositional basin; Whitohouse (1955, fig.35) however viewed these as continuous, through a postulated strait across the Palmer River, with the Blythesdale and Roma sediments of the Great Artesian Basin. They undulate very gently, and the basement on which they lie is regarded as having an irregular erosion surface, and not as being either a peneplane or a plain of marine erosion. Near the Palmer River the erosion scarp at the southern edge of the Basin transgresses apparently without any difference in level, across the Tasman Line, suggesting that 100 Pre-Cambrian shield and Tasman géosynclinal region was acting as a single, welded, stable unit in Mesozoic times. The state Map 1953 suggests that the present Laura Basin is a structural Basin, with its axis running N.W. - S.E. across the more merid ional grain of the augmented craton, and from Ball’s (1909) observations, this attitude may have been imparted by a late Tertiary coastal uplift (his Cook uplift) with which was assoc iated basaltic outpourings along the coast. The oldest Mesozoic formations of the Laura Basin are considered by Denmead (194-9) to be the massive sandstones and conglomerates of Hawkesbury type exposed in the Upper Kennedy River, and these be regarded as freshwater and doubtfully Triassic, no fossils being known from there. Further east, in the Normanby, sandstones and subordinate shales with the thin coals of the Cooktown district lie directly on the Palaeozoic basement, presumably overlapping the ? Trias in that direction^ Ball (I9IO) found Taenionteris and Cladonhlebis leaves in these beds, strong presumptive evidence that they may be correlated with the Walloon Coal Measure of supposed Jurassic age. Ball (1910) also remarked on the discontinuity of individual beds in the Mesozoic sequence. Porous soft sandstones and coarse grits correlated by Denmead, because of their lithological character and water content, with the L, Cretaceous Blythesdale Sandstone of the Great Artesian Basin, lie above these coal-bearing strata between Fairview and Laura, but are apparently either undeveloped, unrecognised, or perhaps overlapped by at least 800 ft, of dark blue marine shales and white sandstones of Aptian (Roma) age west of Fairview, These are the youngest Mesozoic beds known 101 In the Laura Basin, no equivalents of the Albian Tambo Formation of the Great Artesian Basin having been recognised» Ü» 3h the Pascoe River area occur white and yellow sand stones occasionally containing a few pebbles, and lying on a very uneven basement, between the eastward scarp of the Sir William Thompson Range and the coastal ranges (Jack, 1881 and Morton, 1924, 1930)» They are shown on the State Map as Jurassic, are quasi-horizontal, and carry a very poor soil on which grass does not flourish» Some thin coals occur» These are overlain by the 500 ft» reddish sandstones with iron oxide cement of the Sir William Thompson Range, which carry good grass and dip almost imperceptibly westward and northward to the Gulf of Carpentaria, and form part of the Carpentaria section of the Great Artesian Basin» iii. The Carpentaria Section of the Great Artesian Basin, which lies west of the Main Divide in the south, but transgresses the Main Divide south of Temple Bay, is parted into two areas of outcrop by an extensive spread of delta-like siliceous gravels and clays which completely overlap the Mesozoic rocks along the Palmer R», and come to rest there directly against the pre- Cambrian gneisses and granites of the Main Divide (State Map 1953 and Whitehouse, 1955)» Only two Mesozoic formations are recognised in the parts lying both to the north and south of this Tertiary spread, the Blythesdale, and the Roma equivalents» North of the Holroyd R» the 500 ft» ferruginous and siliceou s sandstone of the Sir William Thompson Range mapped as Blythes dale on the State Map, mentioned above in the section on the Pascoe River area, dips almost imperceptibly westwards and 102 northwards, crossing the divide to come down almost to sea level on the east coast to the south of Temple Bay« The Lower Cretaceous plants described by Walkom (1928) from ELutoville in beds just above an unconformity with the granites, probably came from the base of this formation« Just 6J- miles from Cape York Peninsula on the east coast, molluscan shells recorded by Whitehouse (1955) as marine, but ßonsidered by daessner (in litteris 1956) to be of the fresh water Iftiio group, have been collected by geologists of Mt« Isa Mines Ltd« This formation is recorded from the Mb« Adolphus islan d s, capping the basement there, but i s not known further north on any of the Torres Strait islands« Presumably above the Blythesdale sandstones, in the vicinity of Mein Telegraph Station, and 24 miles south of Mo re ton Telegraph Station, Roma fossils are known in marine blue grey clays, but the outcrops of this formation, like those of the Blythesdale, are heavily obscured by latérites and lateritic debris« Morton (1925) was unable to determine whether the dip of the ^lythesdales* was sufficient to carry them under these iRoma* beds« Whitehouse (1955) reports tßlythesdale1 fossils from E« of Rokeby, from a lo cality coloured as tRoma1 on the State Map« He has everywhere interpreted fo ssilife ro u s marine sandstones outcropping along the borders of the Great Artesian Basin as a formation not only distinct from but older than the blue grey clays of the Roma Formation« No palaeontological monograph has been devoted to this sandstone fauna, which appears to d iffe r at most in species, not at a l l in genera, from that of the Roma Formation, and I suggest that in places at least these marine sandstones may be coegal with the Roma blue grey clays 103. but developed as marginal, shallow-water, on-shore facies. From the Mitchell River southwards, the formations of the Carpentaria section may be traced in continuous outcrop to those of the main section of the Great .Artesian Basin. No Mesozoic rocks younger than Aptian have been recognised in Cape York Peninsula, and whether the ALbian Tambo formation, well known in the Great Artesian Basin, was ever laid down there is doubtful» No marine Tertiary sediments are known. The only Tertiary sediments known are the 100 ft. or so of loosely compacted conglomerates or drift sands (which may indeed be Quaternary) overlying the Mesozoic sediment near Fairview in the Laura Basin (Denmead, 1940) and the great spread of siliceous gravels and clays forming the delta like deposit along and between the courses of the Staaten, Mitchell, Palmer, Coleman and Holroyd Rivers, and which may indeed be Quaternary, "since they are only lightly lateritised, and seem in part to be made up of outwash from la té rite s» Laterite is very important in the Peninsula, affecting particularly the tBlythesdale* and iRoma1 of all that section north of the Palmer River» The ferruginous la te r ite surface comes down to sea level in the northern part of the Peninsula, «pad may pass under recent sand dunes and coastal allu v ia. I f one could safely assume that the la te rite was everywhere developed at the same height above sea lev el, in a peneplaned region, one would have a good datum fo r géomorphologie inter- 1Q4 pretation of post laterite earth movements* However, the assumption seems at present too great a one to act on. Basalts occur in small patches in the coastal region of the Cooktown district only. Ball (1909* 1910) reported that they generally occur along the valley bottoms of the present drainage system, and that a cinder cone is still present in the upper Endeavour valley. Denmead (oral communication) reports very steep dips in Mesozoic sandstone in the vicinity of the Little River Permo-Carboniferous coal measures; but insufficient is known about this for assessment. It may be pointed out that the Little River coal field lies between two faults along the old Tasman Line, which can be assumed to have moved repeatedly since the pre-Cambrian. Ball (19 10 ) called the supposed movement elevating the eastern edge of the Laura structural basin the Cook Uplift, and considered it related to the late Tertiary basalts now lying in some coastal velleys there* 105. List of Authors on the Geology of Cape York Peninsula B a ll, I W , 1910 Denmead, 1949 H ill, 1951, 1952 Old. State Map, 1953 Morton, 1924, 1925, 1930 Jukes, 184*7 Rattray, 1869 Haddon, Solías & Cole, 1894 Shepherd, 1944 Jones & Jones, 1956 Jack, 188], 1922 Jack & Etheridge, 1892 Reid, 1930 Jackson, 1902 Walkom, 1928 Whitehouse, 1955 Glaessner in letters, 1956* 106, B ,V . THE GEOLOGY OF THE QUEENSLAND COAST SOUTH OF PRINCESS CHARLOTTE BAY, Since this has been analysed by Hill (1951) in pages of the Handbook of Queensland prepared for the 28th Meeting of A.N.Z.A.A.S., a copy of this paper is enclosed herewith, and should be read at this point of the present report. Since, when the paper was prepared I had not compiled or analysed the known geological information on Cape York Peninsula, which I have subseq* ently published in map form in the Queensland State Map, I have dwelt at length in Section B.IV on the geology of Cape York Peninsula, Such detailed treatment for the rest of the Queensland coastal area is however rendered unnecessary by the Handbooks Geology1, quo vide. 107 B. VI. THE GEOMORPHOLOGY OF THE QUEENSLAND COAST AND STRUCTURAL HYPOTHESES ON THE CONTINENTAL SHELF DEVELOPED FROM IT Perhaps the most striking feature of the Queensland Coast is that it is for much of its length oblique to the geological grain of the country. It cuts obliquely across the various great structural highs and lows. The characteristic trend line of Queensland folds and faults is N.'“. W ., with variations sometimes to the N.W. and sometimes to the N. The coastal ranges in general run with the geological grain, and in many places they appear abruptly truncated by the sea. In other places they appear to plunge under the s ea and be represented by trains of isolated islands. These high islands are mostly separated from the inner barrier reefs by the steamer channel, but a few lie in the steamer channel. Many coastal ranges and segments of coastal ranges are separated by straight edged corridors filled with alluvium whose upper surface is only a little above sea level; other ranges are separated from the sea by alluvial coastal planes, and marine corridors lie between coastal ranges and trains of high islands. Only one sizeable delta occurs along the coast, that of the Burdekin. Headland is separated from headland by a succession of bays with a short E.-W. shore-line and a long N.-S. shore-line giving an angulate effect. Most authors consider the coastline a xyoung* submerged one. No marine Tertiary strata are known anywhere along the coartljn«, and no marine Pleistocene either. Sub-recent marine beds are known in some of the coastal plains. 108 The dominant theme of writers on Queensland coastal morphology, though each individual has his own variation on it, is that a post-Cretaoeous (Taylor) or late Tertiary (post- Miocene of most, post-Pliocene of some) sea-level peneplain extended out at least as ihr as the outer edge of the Great Barrier Reefs, and was uplifted in either one movement or more than one movement in pre-Pleistocene time, the uplift being greatest either on or to the east of the present Main divide, while the coastal region was fractured into blocks which moved differentially, that part under the present continental shelf being depressed the most, and other regions like the coastal corridors and coastal plains, being depressed less* Some of the coastal range blocks moved upwards less than the main inland tableland region did (3 to 4 thousand feet), others more* Authors who have advocated one or other variation on this theme are Andrews (1902, 1910, 1933), Hedley & Taylor (1907), Hedley (1911), Taylor (1911, 1927), David (19H, 1932), Danes (1911), Jardine (1923, 1925a, b, 1928a, b), Richards & Hedley (1925), Stanley (1928a, b), Steers (1929), Sussmilch (1928) and Fairbridge (1950). On some variations (Sussmilch and Stanley), the surface that was thus cut up into blocks was horizontal, in others the surface was tilted to both east and west away from the central N*-S* axis of main uplift (Taylor)* Hedley (1911) saw the uplift as complementary to a deepening of the Carpenter Deep (= Coral Sea Basin)* Fairbridge saw it accompanied by downfaulting outside and along the line of the Great Barrier Reefs ^""om Trinity Opening northwards• 109 Clearly to those who held the above views and dated the supposed fracturing as post-Miocene, nothing but marine Pliocene, Pleistocene and Recent rocks could lie between the hard continental basement under the Great Barrier Reef; and this is one view on the nature of the reef foundations. However, Marks (1924) has rightly and severely criticised both the deduction of a peneplain and the deduction of faulting, pointing out that there has been no geological mapping whatsoever along the coast of sufficient detail or accuracy to support either assumption. In this I agree with him completely. Marks, like Bryan (1930) considers differential erosion quite sufficient to account for the main variations in level along the coastline. Reid (1924 ) also sees no gr^logical evidence for the large scale faulting desired by the proponents of the * fractured coastline* theory. Cotton (1949) removes the late Tertiary dating of the assumed faulting by suggesting that the supposed faults may be fault line scarps, related to more distant movements. This view would permit marine Tertiaries or Mesozoic rocíes to be expected under the continental shelf. Another type of theory is based on theories of the origin of barrier reefs. Thus Darwin suggested that the Barrier Reef has grown upward from a fringing reef during submergence of the coastline, possibly since the Cretaceous (Davis, 1917). Darwin envisaged a tectonic submergence, not a eustatic submergence such as the supposed late Pleistocene rise in ocean level due to the melting of the Pleistocene ice caps. This latter is generally assumed to be of the order of 200 feet, and many no. authors have considered the Queensland coast to be drowned by 100 to 200 feet, the evidence being that coastal rivers are found in their lower courses to be running in the top layers of their own gravels, infilling channels they had previously excavated. (Jack & Etheridge, 1892; Agassiz, 1898; Bryan, 1938). On this type of theory it would be possible to pass through the f u n Tertiary marine sequence and perhaps also part of the Mesozoic in a bore put down on an Outer Barrier Reef. There seems nothing to disprove this possibility, even if Darwin and Davis did not take into account a possible eustatic rise in sea le v e l. Fairbridge, 1950, pp. 376-381 has given a most useful review of the various guesses on the basement of the shelf in relation to the different theories on the growth of coral reefs. Clearly different views on the origin of the Great Barrier Reefs would lead to different views on the foundation on which they rest. An antecedent platform with glacial control of growth by the return of the waters could be entertained fo r a late Tertiary foundered continental peneplain, as supposed by Stanley (1928). Equally, a plain of marine erosion formed during the time the most water was locked up in the Pleistocene ice caps could form the basis fo r new and upward coral growths as the waters returned (Daly). Neither of these two alternatives seems sufficient explanation of the fact that more than 700 ft. of apparently post-Pleistocene sediment was found in the Heron I . Bore and almost as much in the Michaelmas Cay Bore; additional tectonic subsidence has to be supposed on either theory; there is no reason to suppose Tertiary or even Mesozoic HX marine sediments may not be present under the Barrier* Stanley (1928) pointed out the difference in the coral growth north and south of Trinity Opening, and suggested that this marked the southern limit of coral growth during the Pleistocene lowering of temperature and sea level, and this idea has been accepted by Fairbridge (1950), who considers that the line of outer reefs both south and north of this represents the shore line during this period of lowered sea level, but that north of Trinity Opening this shore line was already a young fault scarp* Although the geomorphologists have in general insisted that Pleistocene or at oldest Pliocene marine sediments can be expected at the edge of the Barrier, I cannot accept that they have satisfactorily ruled out the possibility of slow tectonic subsidence of the continental shelf region, and consider that it is not at all impossible that a reasonable sequence of marine Tertiary strata possibly overlying Mesozoic marine might lie below the Queensland continental shelf in regions outside the outermost high islands* I do not think any of the evidence available to us at present is sufficient for us to regard an exploratory deep bore on the outer barrier rs foredoomed to meet basement before passing through several thousand feet of marine strata* That some tectonic subsidence has occurred in addition to rise in sea level by glacial melt waters, is shown by the 700 ft, of sediment already found in the two shallow bores at Heron I, and Michaelmas Cay. How great was this subsidence can only be found by (1) deep boringj 112* (2) interpretation of the value of g obtained by Mr* J* Dooley of the Bureau of Mineral Resources, during his geophysical investigations on the Reefs in 1954-, in the light of the Michaelmas Cay Bore and (!)• List of Authors on Geomorohologv of Great Barrier Reefs (For details see Bibliography) Agassiz, 1898 Andrews, 1902, 1910, 1933 Browne, 1945 Bryan, 1928, 1930 Bryan & Jones, 1945 Cotton, 1949 Danes, 1911 Darwin, David, 1911, 1932 David & Browne, 1950 Davis, 1917 Fairbridge, 1950 Hedley, 1911, 1925 Hedley & Taylor, 1908 Jack & Etheridge, 1892 Jardine, 1923, 1925a, b, : Jensen, 1911 Marks, 1924 Reid, 1924 Richards, 1937 Richards & Hedley,. 1925 Richards & Hill, 1942 Stanley, 1928a,, b Steers, 1929 Sussmilch, 1938 Taylor, 1911, 1927 113 B.VII. MAJOR STRUCTURAL UNITS OF QUEENSLAND IN RELATION TO THE BASEMENT F.YPF.OTTD UNDER THE QUEENSTAND CONTINENTAL SHELF In the view of Hill (1951 — copy enclosed as appendix to the present report) the present coastline of Queensland, from Temple Bay in C. York Peninsula to the N.S.W. border, cuts in general obliquely across the ancient Tasman Geosyncline on to the Pre-Cambrian craton and shield with its horizontal overlying Mesozoic sandstone, to which the present sea is brought in the small section north of Temple Bay (see ink correction to text fig# 1 in Hill, 1951)* The Tasman Geosyncline is divisible into a number of units, alternate structural highs and lows, which are cut across by the remainder of the coastline. Thus the Siluro - Devonian Chillagoe Shelf region is transected at Temple Bay. In the vicinity of Princess Charlotte Bay, the northern end of the Devono-Carboniferous Jack Basin, overlain by the Laura Mesozoic Basin, is cut across. Thence to Townsville the North Coast older Palaeozoic High is at the coast line0 At Townsville the closed head of the Permian Bowen Basin is met* Thence to the Mackay Region, the Palaeozoic Gogango (Bogie) High meets the sea. Prom just south of Mackay to east of Broad Sound the upper Palaeozoic Yarrol Basin with the included ? graben of Cretaceous Styx R. coal measures is very obliquely cut by the coast® South wards from Broad Sound to Baffle Creek the North Coast Lower Palaeozoic High is met, and southwards from Baffle Creek to Sandy Cape, lie the transected Gympie Permian and superimposed Maryborough Mesozoic Basins© 114. Let tis now group the high islands off the coast according to their geology, and see how they relate to the above structural units* North of and in the vicinity of Cape York, the islands are of granite, or of the ignimbrite or the quartz felspar porphyry of the types intruding both the ancient metamorphic rocks of the cf aton and the Peninsula ? extension of the Devono-Carboniferous Jack Basin* They are interpreted as rising from a submerged sedtion of the Pre-Cambrian craton* (Jukes, 1847, Rattray, I 869, Haddon, Solías & Cole, 1894* Jackson, 1902, Richards & Hedley, 1925, Shepherd, 1944, Jones & Jones, 1956)* Between C. Grenville and Princess Charlotte Bay the headlands and high islands, including the Sir Charles Hardy Is* and the Forbes Is* which project through the inner barrier reef region, are granitic or ignimbritic, or acid porphyritic, and could be related to the granites and volcanics of the Siluro-Devonian Chillagoe Shelf region and the Jack Basin* (Rattray, 1869, Richards & Hedley, 1925, Jones & Jones, 1956). The Flinders Is* and Clack I0 on the east side of Princess Charlotte Bay are of grey sandstone without shales, like those regarded as Jurassic at Bathurst Head and in the Laura Basin* The sandstones of these Isles are slightly arched about a N.N.E. - S.S.W. axis, the anticline plunging both to the north and to the south* Richards & Hedley (1925) suggest an eastern source for the particles* From Lookout Pt* and C* Flattery to near Townsville, head lands and the few high islands known are of granite or Lower Palaeozoic metamorphics as in the North Coast High, overlain by 115 the Jurassic sandstones of the Laura Basin only as far south as Cooktown. (Jack & Etheridge* 1892* Jack* 1922). South of 0» Grafton to a little north of Townsville, the high islands and some of the coastal headlands are of granite or pre-Cambrian metamorphics, supposedly brought up in anticlinal cores in the Barron R. Lower Palaeozoic metamorphics (Bryan & Jon?s, 1945, Jones & Jones, 1956). The Palm Is., north of Townsville, are of granite of unknown age relations (Richards MS.). Off Townsville and to C. Upstart, the high islands are of granite intrusive into Permo-Carboniferous volcanics, as above the head of the Bowen Basin on the Mainland (Maitland, 1892).. From Bowen down the coast to the eastern side of Broad Sound the high islands are all granite or upper Palaeozoic volcanics such as are met in the narrow Yarrol Basin of the mainland (Stanley, 1928; Jardine, 1928). To the east of this group there lies a series of marble and rhyolitic islands, such as the Duke Islands and the Percy Isles, (Ball, 1904, Richards MS.) which could well belong to the early Devonian belt of the South Coastal High, since they are similar to rocks outcropping on the mainland in the Mb. Etna district of Rockhampton. Still further east, but south, lie the Keppel Isles, of Brisbane Metamorphics as in the South Coastal High near which they lie (Ball, 1904, Jardine, 1920, R5.chards MS.). Facing I 0, off Gladstone has at Gatcombe Hi, its southernmost point, an outcrop considered pre-Cambrian (Bryan & Jones, 1945), presumably exposed in an anticlinal oore in Brisbane metamorphics 116 reported from neighbouring islands. (Ball, 1904; Jardine, 1923; Richards MS.) and on the mainland nearby, Further south again are the islands in Hervey Bay with marine Cretaceous as in the Maryborough Basin. (Bryan & Jones, 1945). There seems therefore every reason for assuming that the structural units of the coast are continuous under the western part of the continental shelf; but in the zone of the inner and outer barrier reefs, apart from the Hardy and Forbes Is. near Cape Grenville, they do not appear at the surface. Wo have no means of knowing how far below those Barrier Reefs the tops of these old ranges extend, or the bottoms of the intervening valleys. The trend lines of the island trains seem in all cases to follow the structural trends of the related mainland units. Reefs, if based on them, would presumably be aligned on these trends. Unfortunately the lack of naval surveys and aerial photographs of the region between the western edges of the inner barrier reefs and the eastern edges of the outer barrier reefs, for the entire length of the reefs, precludes us from knowing whether such alignments are present or not. Fairbridge (1950) considers alignment of reefs north of Princess Charlotte Bay occurs, and he regards it as parallel to trends in the Hinders Is. However he also points out that the alignment is with the tidal currents here, and this may indicate they are based on sediment trains rather than on hard ridges. Fairbridge (1950) also describes alignment of the Bunker and Cnpricorn Group reefs in the south, and attributes this to their growing on sediment trains elongated in the direction of the prevailing local currents. 117 However, less uncertainty would be experienced if aerial photographs were to hand. From what is known of the geology of the Tasman geosyncline in coastal Queensland, its Palaeozoic rocks are seen to have been so much effected by intrusion, metamorphism and diastrophism as to have at the present time, no oil potential in any extension under the continental shelf, to the later sediments of which they must be regarded as basement* na B. VIII. THE CORAL SEA.. Coral Sea soundings are very few, but indicate several topographic unities to which Fairbridge (1950) has applied convenient names. To the N.E. lies the Papuan Trough of more than 1000 fathoms, deepening southeastwards into the Coral Sea Basin ( = Carpenter Deep). Between this and the Queensland continental shelf from C. Melville to Sandy C. lies the Coral Sea Platform, a rhomboid region rising to 200 fathoms towards the south, but falling gently northwards. From this platform rise the Saumarez, Marion, Iihou, Flinders, Willis I., Bougainville and Osprey Reefs, all of them atolls. Between the Queensland continental shelf and the northern part of the Coral Sea Platform lies the northward deepening Queensland Trench falling from 500 fathoms off Townsville to 1000 fathoms off Trinity Opening. To the south, the slope of the Coral Sea Platform swings soutfci’ostwards and steepens to join the continental slope of Queensland off Sandy Cape, with however a wide gulf known as the Capricorn Channel heading into the lagoon inside the Great Barrier Reefs. South of Sandy Cape the Queensland continental shelf is very narrow and the slope steep. Concerning the geology of the Coral Sea we have the only facts that nothing but coral rock is known rising to the surface from it and that no earthquake shocks are recorded from it (Bryan, 1944)* We have however observations from earthquake travel times (de Jersey, 1946) indicating that sialic crust exists between Brisbane and the Kermadec Is., but that it is only 25 km. thick as against 40 km. for Australia. This seems 119 to show that foundered parts of the continent of Australasia exist under the Coral Sea¿ Officer’s calculations (1955) seem to suggest that 20 km* would be a better estimate for the thickness of the sialic crust. All other views on the nature of the rocks under the Coral Sea are based on views of the relation of the topographic units in the Coral Sea to one or other theory of continental formation or foundering, or one or other theory of orogenic type. Bryan (1944-) has given a complete review of these applications of theory until 1944, the chief papers being by Marshall (1911, 1933) Jensen (1911), Gregory (1930), Schuchert (1916), Sussmilch & David (1920), Benson (1923, 1924) and Andrews (1937, 1938)» Bryan shows that the various theories resolve into two groups, one of the growth of Australia eastwards at the expense of the Pacific, and the other of the foundering of a large continent extending from W. Australia to the Marshall line, the Tasman geosyncline being a median belt of mobility developed within it. Present opinion seems to favour the foundering hypothesis, and Bryan regards the foundering as early Tertiary. Since however stable lands are subjectto epeirogerdc downward movements, under neither set of hypotheses can we draw any reasonably informed deductions on what a bore put down on the Coral Sea Platform would strike. Possibly marine Quaternary and Tertiary, overlying possible transgressive Mesozoic marines, overlying Palaeozoic basemente Since Bryan’s review, other writers have speculated on the nature of the topographic unities of the Coral Sea, without however contributing anything of more secure value. These lines of thought may be followed in Browne (1945, 1949), David .... 120* and Browne (1950); Glaessner (1950, 1952a, 1952b); and Fairbridge (1950a, b). Obviously, what is under the Coral Sea Platform has a bearing on what is under the Queensland continental shelf, but at present we have no facts to go upon. A boring through the Saumnrez Reef would be a real contribution. Literature bearing on the Geology of the Coral Sea Floor Andrews, 1937, 1938. Benson, 1923, 1924-. Browne, 194-5, 194-9. Bryan, 1928, 1944-. David, 1932. David & Browne, 1950. Fairbridge, 1950a, b. Glaessner, 1950, 1952, 1952b. Jensen, 1911. de Jersey, 194-6. Marshall, 1911, 1933. Officer, 1955* Schuchert, 1916. Sussmilch & David, 1920. 121» C. RECOMMENDATIONS FOR EXPLORATORY WORK 1. Surface geological work is not applicable to the barrier area of the shelf outside the zone of high islands. 2. Geophysical work might establish whether faults in the basement occur, along the present N. Queensland coast and along the outer edge of the Barrier north of Trinity Opening, in both of which places they are postulated by geomorphologists* The values for g already obtained by J. Dooley of the Bureau of Mineral Resources might, if worked up, do this without further work* 3* Because of the unsurveyed and unexamined nature of much of the actual barrier area, aerial photography should be undertaken a. to indicate any alignment of reefs, in case this is controlled by structure b* to give some sort of chart for navigation for the use of launches oarrying geophysical apparatus in these dangerous waters* 4# Given reef alignment, geophysical work could be undertaken to establish whether it is due to ridges in the basement or other structure at depth* Such reef alignment or elongation is suggested (a) on the Yorke Platform west of Murray Is*, (b) north of Princess Charlotte Bay and (c) in the Bunker and Capricorn Groups. 5» To me, however, the most direct method of exploration, that of boring, appears called for, to establish the stratigraphic sequence and the porosity of the rocks* Once this is done, geophysical work as in paras (2) and (4) could be undertaken in the vicinity of the 122, exploratory hole or holes which will give the necessary standard. In the sections that follow (C. IX - XIII) I indicate what I consider to be the best sites for such exploratory borings. 123. c. IX* the o il poten tial of the queensland- papua continental SHELF BETWEEN 1 ¿3 ° E, THE GREAT BARRIER REEF. AND THE MERIDIANS OF BRAMBLE CAY AND 11° S« (THE YORKE IS . PLATFORM). WITH RECOMMENDATION FOR AN EXPLORATORY BORING THEREON Having surveyed the geology of the Cape York Peninsula, the Torres St. islands, Papua and the coral-reefs, of the head, o f the Coral Sea, we are in a position to consider the oil potential or the area named, in the heading to this chapter* The deductions of regional structure w ill be listed, to show the conclusions on which the recommendation for a boring is'leased* 1» The crystalline rooks of the high islands in the Torres .. Straits between 142° E. and 142° E> as far N. as Mabaduan H ill and thence N.E* to the Maremosab Boring on the Qriomo R*, .are the northern continuation o f the Cape York Peninsula* basement to the Mesozoic , strata of the Peninsula. 2* This- C* Yorke Paninsular-W. Papuan basement ridge, which we might call the Banks. I, ridge, besides plunging to the N. under ;he Mio-Pliooene-Quaternary strata of W* Papua, fa lls away westward under the Mesozoic and Tertiary strata of the Gulf of Carpentaria section of the Great Artesian Basin, and eastward under the .Kontinental shelf of - Queensland -..Papua. 3-0 "Since, no marine strata older than Miocene are- -known..on this basement in*the Mahaduan-Oriomo area, it-- appears. lik ely that the Aptian*.Albian marine sea of the Great. Artesian Basin-was. flooded from th e -N*W.-or.-N^Nrather than across .the Banks-1*., ridge.«. A* " The Banks 1^. r id g e i s app a ren tly an. a n cie n t s tr u c tu r a l feature,-and may bean 'inheritancQ ..from the- old..Tasman lineament separating Tasman geosyncline from Gratan. 124. 5. If Mesozoic marine strata exist in the Yorke Is. region, they would be related to Gulf of Papua and Coral Sea regions rather than to the Great Artesian Basin. The nearest known Mefeozoic rocks to the YOrke Is4 region is the Cretaceous encountered in the Omati Bores of the Delta Regiom This did not extend as far to the S.W. as Oriomo, and unless the Yorke Platform was flooded by Cretaceous (and perhaps older) seas from the S.E. from the Coral Sea region, we would not expect to find Cretaceous or older Mesozoic marine strata on it. 6 . Since no Eocene or Oligocène rocks are known on the Oriomo shelf, we would similarly not expect to find them on the Yorke Platform unless it was flooded by Palaeogene seas from the Coral Sea. 7* Miocene-Pliocene shelf sediments are known on the Oriomo Shelf, and we might reasonably therefore expect to find them under at least the northern part of the Yorke Platform. 8. If the Warrior Line was a Pleistocene shore line, we might find Pleistocene marine sediments under the Yorke Platform. 9* We would certainly find the Sub-Recent marine sediments under the Yorke Platform that are known inside the Barrier in both Heron Is. and Michaelmaß Cay Bores. 10. It is thus certain that there lies, under the Yorke Is., up to 1,000 ft. of Sub-Recent sediments? it is probable that Pleistocene marine sediments underly these, but we are without means of estimating their thickness, since although the area is a shelf area it may have been subjected to considerable warping. It is possible that a Mio-Pliocene sequence comparable to that of Oriomo lies underneath, and if the Coral Sea was in being at 125 that time, the thicknesses may conceivably be greater than the I5OO ft. in the Oriomo Bores. Whether Mesozoic marine strata lie at depth depends on the history of the Coral Sea on which we have insufficient knowledge to base any firm opinion. 11. The presence of the Murray Is. olivine basaltic volcanoes on the eastern half of the Yorke Platform may indicate an uplift in that vicinity, related to cratonic crustal warping commonly correlated with such vulcanicity. This may have caused some uptilting of the marine strata under the platform towards the Murray I. Line. 12. The weight of the Pleistocene and recent delta sediments in the Gulf of Papua may have compressed and lowered the Neogene and older sediments under the Gulf, causing primary migration of the oil therefrom into reservoir strata. 13* The possible uptilt towards the Murray Is. may have caused secondary migration of this Neogene oil up dip on to the Yorke Platform. 14- If the E. - W. linoation of the reef in the vicinity of Yorke Is. is not purely a reflection of the current control of the shape of banks of sediment, but is related to the very shallow E-W undulations in the Oriomo shelf region, oil may have become trapped under anticlinal caps under the Yorke Is* On the Oriomo Shelf however these undulations were too slight to carry oil and were also filled with water. If however Palaeogene and Mesozoic marine s ediments lie at depth, they would presumably be shelf sediments and would lie up dip from their continuations under the depressed Coral Sea. We are unfortunately without any evidence on which to deduce fold structures in any such strata. 126 15* There is thus no certainty whatsoever that oil or even structure is present under the Yorke Is., but a bore put down there would prove the stratigraphic column for this possible continuation of the Oriomo Neogene belt, and throw light on the history of the Coral Sea Basin, sufficient to take advantage of it here or southwards. 16. The Yorke Islands, Chart Aus. 103, are from the point of view of the practicability of boring, about the best site available on the whole Reef area. North of C. York, tropical revolving cyclones are not known, and to be able to erect and operate the rig without this source of danger is a great advant age. Rigs could possibly be brought from New Guinea. There ore two islands in the group, the larger Masig and the smaller Kodoll, both situated on the same reef, along its northern side. Both are sand cays, the larger being 1-J- miles long and half-a- mile wide, flat, 70 ft. to tops of trees; the latest chart shows a mission station for islanders. They are close to the Great North East Channel, with waters safe for navigation from there to the Channel. If difficulties in connection with aboriginal reservations were encountered, Keats I, a small sand cay about one-third of a mile long on a reef a little north of the Yorke Is, could be used for a boring. 17e Anchor Cay, (Aust, 103) or East Cay, at the extreme N.E. end of the Outer Barrier, might be preferred to Yorke Is. for a site as being nearer to the assumed edge of the shelf, but navigational hazards would be greater, and the cays, being smaller than Yorke Is., less comfortable. 127. C.X. THE OIL POTENTIAL OF THE QUEENSLAND-PAPM CONTINENTAL SHELF BETWEEN C. YORK (approxi 11° S.) and C. MELVILLE (approx. 14° S.) 1. This section of the shelf is possibly too far south to share in the Mio-Pliocene transgression of the Oriomo Shelf of western Papua, if we assume that this flooding came from the north. 2. If, however, we assume that this transgression came from the Coral Sea region, for which there is no evidence at present, Mio-Pliocene marine strata could lie under the continental shelf. 3* We can reasonably expect up to 1000 ft. of Recent and sub-Recent strata, since there is no reason to believe that this portion of the shelf did not share in the probably post-Pleistocene subsidence evidenced by the Michaelmas and Heron borings. 4* Some authors are of the opinion, from geomorphological argument, that Pleistocene coral reefs flourished in this sector. This view is based on the difference in development of reefs north and south of Trinity Opening. If they are correct, we could possibly expect Pleistocene subsidence to have assisted in the growth of the reefs. $. Many geomorphologists consider the C. York coastline a fault coast, and that the shelf subsided down this assumed fracture line in late Tertiary times. Some consider the subsided shelf segment to be part of a continental late Tertiary peneplain; 12S of these some consider this 1 basement1 to lie horizontally* If these latter are correct, we could expect to find only post fracture marine sediments of a thickness equal to the subsidence. Others consider this basement* to be flexed. If these are correct, and the flexing was outwards, we might expect a few hundred feet of additional strata towards the outer edge of the shelf. It must be stated, however, that in my opinion there is no concrete evidence that any such fracturing has occurred; or, if one assumes it did occur, of its age. 6. If we do not assume that the north Queensland coast is a fault scarp and that subsidence of the seaward portion of the land occurred only in late Tertiary times, we are at liberty to consider the Queensland continental shelf a normal one,, and to expect sequences of Tertiary as well as Quaternary marine sedi ments under it. 7. If the Coral Sea was marine during Tertiary times, Tertiary marine sediments may be expected under the shelf. The only * evidence1 against this is Glaessnerfs supposition that granitic land existed west of Port Moresby during the Eocene and Oligocène, in explanation of changos in sedimentary facies during the Eocene and of derived fossils in the Oligocène. 8. The Tasman géosynclinal Palaeozoic rocks of coastal Queensland are so much affected by igneous metamorphism and diastrophic activity that they must at present be regarded as having no oil potential in their extension under the continental shelf and as acting as basement to possible Mesozoic and Tertiary carriers 129 9* This portion of the shelf lies on the northward con tinuation of the Devono-Carb Jack Basin; but although some authors have postulated a graben along this reef, again there is no real evidence in support. Even if the region was a structural low in Devono-Carboniferous times, we cannot assume that this condition continued into later eras, 10. The Laura Basin contains marine transgressive sea deposits of Aptian age. Its deposits are now discontinuous with the coastline and with the Great Artesian Basin which also contains Aptian transgressive deposits, in its main sector and in its Carpentaria sector. Field work on the main dividing range and between the Laura and its neighbouring basins could possibly establish whether their Lower Cretaceous strata were continuous, and whether the Laura Basin was flooded from the west. Such field work could also establish whether there was N/S axial uplift to the Peninsula, 11. If the Laura Basin was not flooded from the west, then it must have been flooded from either the north, from Princess Charlotte Bay along the shelf, or from the east over the shelf. In which case we might expect to meet marine Aptian in any bore put down through the shelf in one or other, or both, of these parts of the shelf. 12. Raine Island, 11° 36 TS. 1 4 4 ° 01*E. a consolidated coral island on the outer barrier (see View on Chart 2354), suggests itself as a site for an exploratory boring on this portion of the shelf. It is far enough north to escape all but unusnnl Queensland cyclones. It is reasonably far from land and high islands (40 miles to the Sir Charles Hardy Is.). A bore put 130 down through it might be expected to pass through about 1000 ft* of sub-Recent coralline material and through Pleistocene coralline material* It could encounter Mio-Pliocene marine; there is nothing to indicate whether Palaeogene would or would not be met. It might meet Aptian marine beds* 13. Sandbank No. S on the outer barrier at 13° 22*S. 142° 43»E is small but vegetated, the vegetation suggesting it is a reason ably permanent bank evidently having resisted storms since 1 8 4 6 or thereabouts. It is however within the cyclone belt, and this immunity might be due for upset, on the law of averages. It is 23 miles E. from C. Sidmouth and could reasonably form the site of an exploratory boring. 1 4 • Sandbank No. 5 at 13° 42*S. 1 4 4 ° 13!E. a small dry cay only a few feet high on the outer barrier lies perhaps furthest from land in this vicinity, and might also receive consideration as a site for an exploratory boring. 15. Nothing can be indicated regarding structure at either * Raine I., Sandbank No. 8 or Sandbank No. 5* The charts indicate an E.N.E. lineation in the inner reefs inside the outer barrier near No. 5 and No. 8; but the survey is far from complete, and the lineation may not be real. If it is, it could indicate either that the reefs are based on trains of sediment elongated in the direction of the prevailing local currents, or that they are based on ridges; such ridges might be either submerged mountain chains (i.e. basement) or they might be growing anticlinal ridges, for which however there is no evidence. 16. If the head of the Coral Sea is deepening (for which we have no evidence) this coulc induce a tilt in the strata of the slope such that oil might migrate, up dip to the edge of the barrier on which Raine I., and the two sandbanks stand. 131 C.XI. OIL POTENTIAL OF THE QUEENSLAND CONTINENTAL SHELF BETWEEN C. MELVILLE (U° S.) and HINCHINBROOK 1.(18° S.) 1, Paragraphs 1 to 8 of the preceding section on the oil potential of the Shelf between C. York and C. Melville apply also to this section of the Shelf. 9. The northern part of this portion of the shelf has the steepest continental slope of the whole of the Queensland Shelf. If the Queensland Trough is deepening or has deepened since the Pleistocene (for which we have no evidence) the largest amount of tilt in the slope sediments may be expected here and any boring put down might take advantage of any migration of oil up- dip. 10. If the Laura Basin was flooded from the East (see Paras. 10 and 11 in previous section), this part of the shelf might carry Aptian marine strata. 11. The only dry cay existing on the outer barrier in this section is the small, 2 ft. high Sandbank No. 1 in 14° 12’S. 1 4 4 ° 53*E. on the reef on the south side of Waterwitch Passage. This however is rather near to Sandbank No. 5 (see para. 14 of preceding section) which is perhaps preferable as a site for an exploratory boring« 12. It might be advisable to make an exploratory boring 132. through the shelf In about 15° S •, • opposite the steepest continental slope of Queensland. Harrier Reef 15° 08*S. 145° 4-11E . just inside the outer barrier near Lark Pass presents itself as a possible site; it had a small sand cay on its N. side during early surveys, but this is not shown on Chart 2923, 1952 Reprint. If the cay has been washed away, engineering difficulties would be encountered; since the reef flat is awash. 13. Any bore along this section of the shelf might expect to meet 1000 ft, of sub-recent sediments, and an unknown thickness of Pleistocene probably coralline material. Below that depth there is no evidence on which to base estimates. If the shelf is a normal type, not one of late Tertiary fracturing and sub sidence of a land surface, marine Tertiaries could be encountered; it is just possible also that the Lower Cretaceous sea entered the Laura Basin over this shelf. 133 C.Xll, OIL POTENTUL OF THE QUEENSLAND CONTINENTAL SHELF BETWEEN HINCHINBROOK I. (18°S.) and PT. CLINTON (22° 2Q*S.) 1« . In this region the outer barrier reefs are not linear reefs, but are patch reefs like the inner reefs of the section north of Trinity Opening; and they stand in 30 or 40 fathoms of water well back from the 100 fathom line and from the continental slope. Fringing reefs are fewer* 2. In this region, too, the Coral Sea Platform practically merges with the Queensland continental shelf, so that their history seems closely related. The continental shelf here becomes very wide, and north of Curtis I. high islands are not found to eastward of 151° E. 3* The geomorphological theory of late Tertiary continental fracturing is more difficult to sustain in this region, since a submarine scarp is no longer found at the outer barrier. 4* There are three regions of interest in relation to possible Lower Cretaceous marine strata on the shelf. (a) Dr. Isabel Cookson has discovered phytoplankton in some bores in Coal Measures in the Cretaceous Styx R. Basin, and advises that they could indicate brackish conditions therein, while not proving this condition. If the sea entered the Styx R. Basin, it presumably did so via Broad Sound region; and if it did, marine Cretaceous strata may lie on the shelf hereabouts. (b) Neocomian (Valangi ar_' very early Cretaceous marire sandstones are known at Kalappa, in the Stanwell district near Rockhampton (Whitehouse, 1942). This horizon is unrepresented ...... 134 as a marine horizon in the Great Artesian Basin, consequently it is probable that the sea entered the Rockhampton area from the east across the shelf, or from the north via Broad Sound. Either way, there is possibly therefore marine Cretaceous in the shelf. Jardine (1923) also has supposed Cretaceous sandstone to be present at Mackenzie I. at the mouth of the Fitzroy R„, but there is no real evidence for this. (c) The Maryborough Basin has recently been shown by the Lucky Strike Co. to contain 6000 ft. of Lower Cretaceous marine strata. This Basin has its northern edge coming out northwards to the coast near the mouth of Baffle Ck., and may continue northwards so as to underly the Bunker and Capricorn Groups. 5« It seems to me very possible that the Bunker and Capricorn Groups and the Swain Reefs lie on a marine Lower Cretaceous continuation of the Maryborough Basin, and that exploratory bores on each side of the Capricorn Channel would be justified to discover whether this is so, 6c It could be that marine conditions continued in the vicinity of the Capricorn Channel since the Lower Cretaceous. 7. The Heron I. Bore proved 700 ft. of marine strata, probably all post-Pleistocene. It does not seem impossible to me that, if deepened to capacity, it could have passed through a marine Tertiary sequence and down into a lower Cretaceous marine sequence before being likely to meet brsement, 8, A deep exploratory bore through any of the Bunker or Capricorn Groups could establish the sequences in this promising southern part. 135 9« North-West Island (23° 18’S. 151° 42*E,), the largest of the cays in the Capricorn Group (400 acres) is recommended as a site. It is on a N.W, trending group of reefs each of which is elongated more E.-W. This may indicate that the reefs originated on banks of sediment elongated in the direction of the prevailing local currents; but it could possibly indicate structure, 10, A deep exploratory boring through the Hixson Cay (22° 21’S, 152° 40*E.) in the Swain Reefs could establish the sequence on the eastern side of the Capricorn Channel, Being further out to sea, presumably, if this part of Queensland1 s continental shelf is a normal one, it is most likely to have the thickest sequence of marine strata, and may be found to have a good Tertiary and even Mesozoic sequence, 11, In case both the sites for exploratory bores recommended in paras, 9 and 10 above, are outside the Company’s authorities to prospect, an alternative might be found in Bell Cay 21° 46’S, 151° 16*E, which lies at the head of the Capricorn Channel, and is the only known cay in this part of the shelf. Aerial reconnaissance might discover others, but the Swain Reefs, except for the vicinity of Hixson and Bell Cays, are unsurveyed or un examined 136 C.Xlll. CONCLUSIONS ON OIL POTENTIAL OF THE QUEENSLAM).PAPUAN SHELF AND RECOMMENDATIONS FOR EXPLORATORY BORINGS 1* It cannot be said that any sites are of better than exploratory potential at present* 2* An exploratory bore in the Yorke Is., 9° 45'S. 143° 25'E. or in Anchor or East Cays nearby would test the theory that marine Mio-Pliocene, as at Oriomo R., W. Papua, lies under Pleistocene and recent marine strata on the Yorke I* Platform. Chart Aus* 103. 3« An exploratory bore through Raine I. (11° 36*S. 144° Ol’E.) would test the prohibitory theory that the Queensland continental shelf has a basement at shallow depth consisting of a subsided late Tertiary continental peneplain. If this theory were disproved the bore could test whether the shelf were a normal one, with marine Tertiary and Cretaceous strata* Chart 2354. 4. An exploratory bore through Sandbank No* 8 or No* 5 (vicinity 13° 30*S.) would perform the same service as in para 3, and also indicate whether the Laura Basin marine L. Cretaceous sea transgressed through Princess Charlotte Bay. Chart 2921. 5* A bore through an outer or inner reef in the vicinity 15° would likewise perform the same service as in para 3, and would indicate what benefit is given by proximity to the steepest continental slope along the Barrier, but engineering difficulties would be encountered here. Chart 2923* 6o A bore through Northwest I. (23° 18*Sa 151° 42!E.) would indicate whether the Maryborough marine Cretaceous Basin is 137 continuous to sea northwards, and could tap the early Cretaceous strata of the sea feeding the Stanwell district near Rockhampton. Chart Aus. 162, 7. A bore through HixsonCay 22° 21*S. 152° 4-0*E. could indicate whether the Maryborough marine Cretaceous Basin extends to east of the Capricorn Channel, and whether this is a 'normal1 portion of the Shelf. Chart 346. 8, A bore through Bell Cay 21° 46*S. 1$1° 16*E. could test the southern area if Northwest I. and Hixson Cay we re outside the Companies authority to prospect. Chart 346* In order of attractiveness, I place these sites: i. Yorke Is. ii. Hixson Cay iii. Northwest I. iv. Bell Cay Y. Raine I. vi. Sandbanks No. 5 or 8 vii. Harrier Reef. 138. D. REFERENCES. AGASSIZ, A., 1898. A visit to the Great Barrier Reef of Australia in the Steamer '’Croydon11 during April and May, 1896. Bull. Mus, comp. Zool. Harvard. vol. 28, No. 4, pp.95-148, pis. 1 -4 2 . (Believed continental shelf had been more or less stationary since the Cretaceous, and concluded that the reefs probably represent only a thin veneer on the shelf. Some 120 ft. thick.) ANDREWS, E.C., 1902. Preliminary note on the geology of the Queensland boast, with reference to the geography of the Queensland and New South Wales Plateaux. Proc. Linn. Soc. N.S.W., 27, pp. 146-185. (Discusses supposed Tertiary peneplains and supposed late Tertiary coastal fracturing.) ANDREWS, E.C., 1910. Geographical unity of East Australia in late and post-Tertiary time. J. Proc. roy. Soc. N.S.W.. 44, pp. 420-480. * (As for Andrews, 1902.) ANDREWS, E.C., 1933. The origin of modern mountain ranges, with special reference to the eastern Australian highlands. Proc. rov. Soc. N.S.W.. 67, pp. 251. (As for Andrews, 1902.) ANGL0-PERSIAN OIL CO., 1930. The oil exploration work in Papua and New Guinea, 1920-1929. 4 vols. (Essential for any geological discussion on Papua ' and New Guinea.) 9 ANON. Sailing directions for the ports and harbours of Queensland. Govt. Printer, Brisbane. (Tides and currents.) BALL, L.C., 1901. The Hamilton and Coen Gold Fields. Geol. Surv. Queensl. Publ. 163, pp. 1-28, 2 maps. [ Between L.Laura R. and Station Ck. a red conglomerate (presumed U. Cret.) sometimes seen, and a mile or so south of the Kennedy a belt of dark-blue impure limestöne; with septarian nodules. Granite appears 10 miles N. of the Morehead. ] BALL, L.C., 1904. Certain iron ore, manganese ore and lime stone deposits in the central and southern districts of Queensland. Geol. Surv. Queensl. Pub. 194, pp. 1-66, maps 1-27, pis. 1-16. (Discussion Duke Group, Islands in Keppel Bay and Pt. Curtis.) 139. BALL, L.C., 1909. The Starcke Goldfield. Geol. Surv. Queensi. Pub. 223, pp. 1-47, 2 maps, 13 figs. (The Mesozoic sandstones of the Laura Basin discussed.) BALL, L.C., 1910. Certain mines and mineral fields in North Queensland. Geol. Surv. Qu^ensl. Pub. 222, pp. 1-53, maps and sections. (The Mesozoic sandstones of the Laura Basin discussed.) BELTZ, E.W., 1944. Principal sedimentary basins in the East Indies. Bull. Amer. Assoc. Petrol. Geol. 28, pp.1440-1454. (Discusses Papuan geosyncline on p.1454 and figures Aure Trough.) BENSON, W.N., I923. Palaeozoic and Mesozoic seas in Australasia. Trans. N.Z. Inst., 54, pp. 1-62. (Discusses Coral Sea, etc.) BENSON, W.N., 1924. The structural features of the margin of Australasia. Trans. N.Z. Inst.. 55, pp. 99-137. BROWNE, W.R., 1945« An attempted post-Tertiary chronology for Australia. Proc. Linn. Soc. N.S.W.. 70, pp. v-xxiv. BRIAN, W.H., 1925. Earth Movements in Queensland. Proc. rov. Soc. Queensl.. 37, pp. 3-82, 4 text figs. (Analysis of trend lines; Pre-Cambrian metamorphics in Barnard Is., etc.) BRYAN, W.H., 1928. The Queensland Continental Shelf. Rept. G t . Barrier Reef Cttee.. 2, pp. 58-69, text-figs. 1, 2. (Orographic, geologic and tectonic relations.) BRYAN, W.H., 1928. Metamorphic rocks of Queensland. Rept. Hobart meeting. A.A.A.S. (Barnard metamorphics) BRYAN, W.H., 1930. The physiography of Queensland, in Handbook for Queensland. Aust. & N.Z. Ass. Adv. Sei.. pp. 17-20. (Discounts the tectonic relief theory for the coastal ranges and considers dissection to play the major part) BRYAN, W.H., 1936. The supposed deepening of the sea floor off Breaksea Spit. Rept. Gt. Barrier Reef Cttee, 4, pp.45-50. (Quotes Edgell's opinion that ’Moresby's survey is the only one deserving credence. Discounts idea of change in bottom topography.) 139 (a). BRYAN, W.H., 193B. Thé pebbles on my garden path. Queensl. Nat.. 10, pp. 83-93. (Drowning of the Brisbane R. Valley.) BRYAN, W.H., 1944. The relationship of the Australian continent to the pacific Ocean - now and in the past. J. Proc. roy. Soc. N.S.W., 78, pp. 42-62. £ Quotes de Jersey as saying that the area between Brisbane and the Kermadec Is. consists of sial but in a layer of 25 km. (as against 40 for the rest of Australia). Disagrees with theories of eastward marginal growth of Australia and of progression welding. Considers Australia and Coral Sea and outlying islands as far as Marshall line to have been continental from early Pre-Cambrian throughout Palaeozoic and Mesozoic eras, and that it broke up in early Tertiary times. Î BRYAN, W.H. and JONES, O.A., 1945. The geological history of Queensland. A stratigraphical outline. Pap. Dept. Geol. Univ. Queensl.. 2, N.S., No. 12. CAMERON, W.E., 1907. Some goldfields of the Cape York Peninsula. Geol. Surv. Queensl. Pub. 209, pp.1-21. CAREY, S.W., 1945. Notes on the Cretaceous strata of the Purari River, Papua. Proc. roy. Soc. Vic.. 56, pi.2. CHAPMAN, F., 1931. A report on samples obtained by boring into Michaelmas Reef, about 22 miles N.E. of Cairns, Queensland. Rept. Gt. Barrier Reef Cttee. 3, pp. 32-42, pis. IX - X. (Lists of names only; no evaluation.) COTTON, C.A., 1949. A review of the tectonic relief of Australia. J. Geol.. 57, pp. 280-296. (Regards the scarps that appear to have bounded horsts and grabens on the coastal belt as possibly fault line scarps related to dislocations more ancient than late Tertiary.) CUMBRAE-STEWART, F.W.S., 1930. The Boundaries of Queensland with special reference to The Maritime Boundary and the "Territorial Waters Jurisdiction Act, 1878". A paper read before the Austral asian Association for the Advancement of Science, Section E. History, at Brisbane, 29th May, 1930, and published by the University of Queensland. Brisbane, pp. 1-18, 1 map. 140. CUSHMAN, J.A., 1942. A report on samples obtained by the boring at Heron Island, Great Barrier Reef, Australia. Rept. Gt. Barrier Reef Cttee.. 5, pp. 112-119, pis. xi-xii. (Foraminifera in cores and deductions on environment.) DANES, J.V., 1911. On the physiography of Northeastern Australia. Próo. ray. Bohem. Soc. Sei. English typewritten copy in reprint collection of Geology Dept, of the University of Queensland. (Agrees that there was a late Tertiary peneplain and that uplift caused a new cycle to begin.) DAVID, T.W.E., 1911. Notes on some of the chief tectonic lines of Australia. J. Proc. roy. Soc. N.S.W.. 45 > pp. 4^-60. (Shows a fault running N. from Princess Charlotte Bay and describes continental shelf to E. as a foundered area. Ditto for shelf off Cairns. Shows also a fault passing into the continental shelf from Broad Sound, and another through Port Curtis. Rightly criticised by Marks, 1924, for insufficiency of evidence.) DAVID, T.W.E., 1 9 3 2 . Explanatory notes to accompany a new geological map of the Commonwealth of Australia. DAVID, T.W.E. and BROWNE, W.R., 1950. The Geology of the Commonwealth of Australia: 3 vols. London. Edward Arnold. DAVIS, W.M., 1917. The Great Barrier Reef of Australia. Amer. J. Sei.. 44> pp. 339-350. (Islands of Bowen District show submergence.) DENMEAD, A.K., 1949. Water search Olive Vale Station, Laura. Queensl. Govt, min* J., pp. 1-2. (Mesozoic sandstones, Laura Basin.) EDGELL, J.A., 1928. Some remarks on coral formations. Rept. Gt. Barrier Reef Cttee., 2, pp. 52-56. 1 sketch. (Process of reef formation.) EDGELL, J.A., 1928. Changes at Mast Head Island. Rept. Gt. Barrier Reef Cttee. 2, p.57. (Reef processes) EDWARDS, A.B., 1950. The Petrology of the Miocene sediments of the Aure Trough, Papua. Proc. roy. Soc. Vic.. 60, pp.123-148. (Greywackes are terrestrial andesitic tuffs redistributed in a marine environment.) 141. EDWARDS, A.B., 1950. The petrology of the Cretaceous greywackes of the Purari Valley, Papua. Proc. roy. Soc. Vic.. 60, pp. 163-171. (Purari Formation = 5,000 ft. massive to thick bedded greywackes interstratified with thin bedded mudstones.) EDWARDS, A.B. and GLAESSNER, M.F., 1953* Mesozoic and Tertiary sediments from the Wahgi Valley, New Guinea. Proc. roy. Soc. Vic.. 64, pp. 93-112, pis. 3. FAIRBRIDGE, R.W., 1950. Recent and Pleistocene coral reefs of Australia. J_. Geol., 58, pp. 330-401, pis. 1-8, text figs. 1-12. (a very valuable review.) FAIRBRIDGE, R.W., 1950. Problems of Australian geotectonics. Scope. 1, No. 5, pp. 22-29. (Coral Sea described.) FAIRBRIDGE, R.W. and TEICHERT, C., 1945. The Low Isles of the Great Barrier Reef: a new analysis. Geogr. J. Ill, pp. 67-88, pis. 1-6, 1 map. (Reef processes.) FISHER, N.H., 1944. Outline of the Geology of the Morobe goldfields. Proc. roy. Soc. Queensl.. 55, pp. 41-80. FLINDERS, M., 1814. A voyage to Terra Australis, undertaken for the purpose of completing the discovery of that vast country and prosecuted in the years 1801, 1802 and 1803 in H.M.S. 'Investigator*. G. & W. Nicol. London GLAESSNER, M.F., 1943. Problems of stratigraphic correlation in the Indo-Pacific region. Proc. roVi Soc. Vic.. 55, pp. 41-80. (A very valuable review.) GLAESSNER, M.F., 1945. Mesozoic fossils from the central highlands of New Guinea. Proc. roy. Soc. V i c ., 56 (n.s.), pp. 151-168. GLAESSNER, M.F., 1949. Mesozoic fossils from the Snake R., central New Guinea. Mem. Queensl. Mus.. 13, pp. 165-181, pis. 14, 15. GLAESSNER, M.F., 1950. Geotectonic position of New Guinea. Bull. Amer. Assoc. Petrol. Geol., 34, pp. 856-881. (A very valuable review.) GLAESSNER, M.F., 1952. The Geology of the Tasman Sea. Austral. J. Sei«, 14, pp. 111-114. (Reference to Coral Sea.) GLAESSNER, M.F., 1952. Geology of Port Moresby, Papua. Sir Douglas Mawson Anniversary Volume. Uhiv. Adelaide. pp. 63-86, map and fig, [[■Nothing older than Upper Cretaceous mentioned. No pyroclastic rocks in U. Cretaceous (Senonian). He gives a diagram showing a pre-Senonian folded basement, on which Senonian is unconformable. J GREGORY, J.W., 1930. The Geological history of the Pacific Ocean. Quart. J. geol. Soc., 86,pp. lxviii et seq. (Has a bearing on the geology of the Coral Sea.) HADDON, A.C., SOLLAS, W.J. and COLE, G.A.J., 1894. On the geology of Torres Straits. Trans, roy. Irish Acad., 30, pt.XI, pp. 419-476, pis. 22-25. (Valuable for geology of islands. ) HEDLEY, C., 1911. A study of marginal drainage. Proc. Linn. Soc. N.S.W., 36, pp. 13-39. [ Suggests Carpenter Deep (apparently = Coral Sea Basin of Glaessner) deepened when post-Miocene uplift took up C. York Peninsula, etc.3 ’ HEDLEY, C., 1925. The natural destruction of a coral reef. Rept, Gt. Barrier Reef Cttee.. I, pp. 35-40, pi. V. (Processes of destruction, coral reefs.) HEDLEY, C„, 1925. A raised beach at the North Barnard Islands. Rept. Gt„ Barrier Reef Cttee., I, pp. 61-2, pis. viii-x. (Geology of coastal islandsj emergence.) HEDLEY, C., 1 9 2 5 . The Townsville Plain. Rept. Gt. Barrier Reef Cttee.. I, pp. 63-65: pis. xi-xiii. (Coastal geologyi evidence of submergence and recent uplift. ) HEDLEY, Co, 1 9 2 5 » A disused river mouth at Cairns. Rept. Gt , Barrier Reef Cttee., I, pp. 69-72, pi. xvii, 1 text fig. (Coastal geology ) iTOLEY, C,, 1925, The Queensland earthquake of 1918. Rept. Gt. Carrier Reef Cttee., I, o p c 151-156. (Epicentre on continental shelf, N. of Hervey B., E.S.E. of Keppel B. ) 143. HEDLEY, G. and TAYLOR, T.G., I908. Coral reefs of the Great Barrier,■Queensland! a study of their structure, life distribution and relation to mainland physiography« Rept3 11th meet« Aust. Adv. Sei « pp. 397-413o T Considered tectonic rocking occurred, at the close of the Tertiary, about the main mountain axis (N0 & S.) of N.S.W. and Queensland, leading to depression in the east and elevation in west (Gulf of Carpentaria and W. Victoria), j HENDERSON, D.A., 1931« Subsidence of the continental shelf northwards of Sandy Cape. Repto Gt« Barrier Reef Cttee., 3* pp P 43-45, 1 text-figo (Successive soundings indicate 100 fathom line migrating westwards; i«e. a deepening of the sea floor No of Breaksea Spit. Refuted by Bryan, 1928.) HENDERSON, D.A., 1951® Morinda shoal, Rept. Gt. Barrier Reef Cttee., 3, p.46, text-fig, 1 , (Circular or oval shoal of 10 fathoms - 19° 08*S. ) HOGAN, J», 1925. Record of sea temperatures observed at Willis Island during the cyclone season of 1922-1923. Rent. Gt. Barrier Reef Cttee., I, pp. 41-46, fig. 1. ( Geology of Coral Sea Platform Reefs ) IREDALE, T., 1942. Report on Molluscan content of Heron Island Reef boring samples. Rept. Gt. Barrier Reef Cttee., 5, pp. 120-122, JACK, R,Le, 1881. On Explorations in Cape York Peninsula. Gaol. Surv. Queens1 . Pub. 8, pp. 1-46. JACK, R.L«, 1922c Norfhmost Australia, 2 vols. Brisbane. ( Numerous geological notes and quotations on 0« York Peninsula and islands. ) JACK, R,L,, and ETIERIDGE, R,, I892, Geology and Palaeontology * of Queensland and New Guinea. Geol. Surv. Queensl. ,Pib. 92, 2 vols, and map, JACKSON, C.F.V., 1902, On a visit to the West Coast of the Cape York Peninsula and some islands of the Gulf of Carpentaria; also reports on the Horn Island and Possession Island Goldfields, and the recent prospecting of the Cretaceous coals of the Cook District; with four maps and twelve plates. Geol, Surv. Queensl. Pub, 180, pp-. 1-2? o JARDINE, F., 1923o The physiography of the Lower Fitzroy Basin. Queenslo geogr, J., 38, ppt 1-42. ( Geolog;/ of Islands )c 144 JARDINE, F., 1925* The physiography of the Port Curtis district. Rept. Gt. Barrier fieef Cttee.. I, pp. 73-110, 8 text-figs. (Coastal geology; geology of coastal islands; emergence) JARDINE, Fo, 1925e The development and significance of benches in the littoral of eastern Australia. Rept. Gt. Barrier Reef Cttee». I, pp, 111-130, pis, xviii-xxii, 8 text-figs* (Geology of coastal islands and headlands; emergence) JARDINE, Fo, 1925* The drainage of the Atherton Tableland. Rent. Gt. Barrier Reef Cttee. r I, pp. 131-148. pis. 23-25, 3 text-figso (Coastal geology; emergence) JARDINE, F., 1928o The topography of the Townsville littoral. Rept * Gt. Barrier Reef Cttee.. 2, pp. 70-87 pis, i-iii, text-figs. 1-4. (Coastal geology; evidence of uplift 19 ft.; evidence of submergence + 100 f t . ) JARDINE, F ., 19280 The Broadsound drainage in relation to the Fitzrcy R. Rept. Gt.Barrier Reef Cttee.. 2, pp. 89-92, p is . iv , V , text-fig. I. (Coastal geology; evidence of uplift) JARDINE, Fo, 1928. Bramble Cay, Torres S tra it. Geological Noteso Rept. Gt* Barrier Reef Ctteeo 2, pp. 93-100, pis. vi-vii, text-figs. 1-3. (Geology islands; ¿eef processes; phosphate) JARDINE, Fo, 19280 Darnley Island - Geological and topographical notes. Rept. Gt. Barrier Reef Cttee.. 2, pp. 101 -109, pis. viii-ix, text-figs. 1-*-3 . (Geology of islands) JENSEN, H.I., 1911. The building of eastern Australia. •££22« ZQY» Soc» Queen s i , 23, pp. 149-198. (Has a bearing on the geology of the Coral Sea) do JERSEY, N.J., 1946. Seismological evidence bearing on crustal bnickness in the South-west Pacific. Pap. Dept. Geol. Lilly e Queer si 0. 3 (N.C.), ITo. 2, pp. 1 —180 (Sialic crust between Brisbane and Kermadec Iso estimated as at 25 Kin. against AO Km. for Australia. Tils indicated continental foundering.) 145 JONES, 0 .A. and JONES, J.B., 1956* Notes on the Geology of some North Queensland Islands* Parts I and II* Rent* Gt. Barrier Reef Cttee*. in press* (A valuable review*) JUKES, J.B*, 1847. Narrative of the surveying voyage of H.M.S. ^ y 1. T. & W. Boone. London. KING, P.P., 1827* Narrative of a survey of intertropical and western coasts of Australia, 1819-22* London. IxENOXi-GQNYNGHAM & POTTS, 1925* The Great Barrier Reef. Geogr. 65,pp* 314-334* (General; description of Murray Is*) MACGILLIVRAY, J*, 1852. Narrative of the voyage of H.M.S. 1Rattiesnake1• T. & W. Boone. London. MAITLAND, A.G., 1891* The Geology of the Cooktown District. Geol. Surv* Queen si. Pub. 70. (Laura Basin sediments) MAITLAND, A.G. 1892. On the geology of Magnetic Island. Geol. Surv. Queensi. Pub. 75* MAITLAND, A.G., 1892. Geological observations in British New Guinea in 1891. Geol. Surv. Que en si. Pub. 85. MA.ITLAND, A.G., 1905* The salient geological features of British New Guinea. W.A. Nat. Hist. Soc., 26 pp. MARKS, E.O., 1924* Some doubts in Queensland physiography. Proc, rov. Soc. Que en si. 36, pp. 3-1S. (Shows there is no real evidence for peneplains or faults between supposed differentially moved blocks; "suggests ordinary erosion as agent.) MARSHALL, P., 1912. Presidential Address to Section C. Rept. 13th Meeting Aust. Ass. Adv« Sei., pp. 90-99* (Has a bearing on the geology of the Coral Sea) MARSHALL, P., 1931* Coral Reefs - rough water and calm water types. Rent. Gt* Barrier Reef Ctteec. 3, PP* 64-72, text-figs. 1,2. (Reef processes; comments on absence of Lithothamnium ridge on reefs inside Barrier, and says calm water type) MARSHALL, P., 1933* Stability of lands in the South-west Pacific. Rept. 21st Meet. Aust. N*Z. Ass. Adv* Sei.. pp .410-411* (Has a bearing on the geology of the Coral Sea) 146 MARSHALL, P., RICHARDS, H.C., and WALKOM, A.B., 1925* Recent emergence at Holboume Island, Great Barrier Reef. Rept. Gt. Barrier Reef Cttee. I, pp. 29-34, pis. iii-iv. (Emergence; geology of islands; Phosphate deposits.) MARSHALL, S.M. and ORR, A.P. 1931* Sedimentation on Low Isles reef and its relation to coral growth. Sei. Repts. Gt. Barrier Reef Exped. 1928-29* 1* pp. 93-133* 3 pis., 7 text-figs. McNEILL, F.* 1955« One Tree Island - remote outpost of the Capricorns. Austral. Mus. Mag.. XI* pp® 333-337. McNEILL, F., 1955* Coral paradise of One Tree Island. Austral. Mas. Mag.. XI, pp® 404-408. (General interest.) MONTGOMERY, J.N., OSBORNE, N. and GLAESSNER, M.F., 1944. Explanatory notes to accompany a geological sketch map of eastern New Guinea. Directorate of Research, L.H.Q., Melbourne, pp. 1-32, map. (Very important map) MONTGOMERY, J.N., OSBORNE, N. and GLAESSNER, M.F., 1950. Outline of the Geology of Australian New Guinea, pp. 662-685 in Sir T.W.E. David, Geology a£ Australia Vol. I (edited by W.R. Browne). M00RH0USE, F.W., 1933* The recently-formed natural breastwork on Low Isles. Rent. £t. Barrier Reef Cttee.. 4, pp. 35-36, pis. vi-viio (Reef processes.) M00RH0USE, F.W., 1936. The cyclone of 1934 and its effect on Low Isles, with special observations on Porites. Rent. Gt. Barrier Reef Cttee., IV, pp. 37-44, pis. viii-xi» (Reef processes.) MORTON, O.C., 1924. Geology and Mineral Occurences, Pascoe River District, Cape York Peninsula. Que en ^ . Govt, min. J., 25, P?. 78-83, 129-134. (Carboniferous sediments, post-Carboniferous quartz felspar porphyry, Mesozoic sandstones.) MORTON, C.C., 1930® Batavia River gold diggings, Cape York Peninsula. Queen si. Govt, min. J., 31, pp. 452*455; 492-498o (Carboniferous sediments, post-Carboniferous quartz felspar porphyry, Mesozoic sandstones.) 147 MOSELEY, H.H., 1092. Notes by a naturalist. An account of observations made during the voyage of H.M.S. Challenger*• John Murray. London. (Torres St. Islands.) OFFICER, C.B., 1955« Southwest Pacific crustal structure. Trans. Amer. Geonhvs. Union. 36, pp. 449-459« (From this it would appear that the Coral Sea sial may have a thickness of 20 rather than 25 km.) OGILVIE, C. and WELLER, N.H.E., 1949* Report on utilisation of the water resources of the Torres Straits Islands, Queensi » Irrigation and Water Supply Commission* OSBORNE, N., 1945* The Mesozoic stratigraphy of the Fly River headwaters, Papua. Proc. rov. Soc. Vic., 56 (N.S.), pp. 131-148. PARADICE, W.E.J., 1925. The pinnacle- or mushroom-shaped coral growths in connection with the reefs of the outer barrier. Rept.Gt. Barrier Reef Cttee.. I, pp. 52-60, 9 sections, pis. vi, vii; frontispiece. (Profiles through reef; reef processes; reef morphology) PARADICE, W.E.J., 1928. The divergence of the ends of the Great Barrier Reef from the coast. Rent. Gt. Barrier Reef Cttee., 2, pp. 110-111. (Geomorphology, form related to silt from rivers, being pushed out where lots of silt, and to currents of Torres St.) RADE, J., 1953. Tectonics and associated volcanic activity in the central part of Australian New Guinea. Austral. J. jj>ci., 15, pp. 115-117. RANDS, W.H., 1892. Report on geological specimens from New Guinea. Anq. Rept. British jjfew Guinea. 1890-91« RANDS, W.H., 18960 Report on the Horn Island Goldfield. Geol. Sprv. Queen si. Pub. 112. RATTRAY, A¿, 1869« Notes on the Geology of the Cape York Peninsula, Australia» Quart. J 0 geol. Soc.. 25, pp. 297-305« REID, J.H., 1924« Tertiary unity or disunity in Queensland. Rept. Meeting Austral. N.Z. Ass. Adv. Sei. REID, J.H., 1930o The Queensland Upper Palaeozoic Succession. Geol. Surv. Queen si. Pub. 278, pp«. 1-95. RICHARDS, H.C., 1938,. Boring operations at Heron Island, Great Barrier Reef. Renta Gt. Ba._rier Reef Cttee«. 4, pp« 135-142 pi. xv. (Record of core; description of island.) 148 RICHARDS, H.C., 1937. Some problems of the Great Barrier Reef, J. Proc, roy. Soc. N.S.W., 71, pp, 68-85 (General) RICHARDS, E.C. and HEDLEY, C., 1925, A geological reconnaissance in north Queensland, Rent. Gt. Barrier Reef Cttee.. I, pp, 1-28 pis■ i-ii, 8 text-figs, and 1 section. (Geology of coastal islands; geology of headlands.) RICHARDS, K.C, and HILL, D., 1942, Great Barrier Reef bores 1926 and 1937 - Description^, analyses and interpretations. Rent. G t . Barrier Reef Cttee., 5, pp, 1-111, plë. i-x; with appendices by J,A. Cushman and T* Iredale. RICKWOOD, F.H., 1955. The geology of the western highland^ of Now Guinea. J. geol. Soc. Austral.. 2, pp. 63-82, 4 pis* and 2 figs. SAVILIE-KENT, W . , 1893* The great Barrier Reef of Australia, London. W.H. Allen & Gg., 387 pp. SCHUCHERT, C,, 1916. The problem of continental fracturing and. diastrophism in Oceánica. Amer. J. Sei.. 42, pp. 91-105. (Has a bearing on the geology of the Coral Sea,) SHEEHERD, S.R.L,, 1936. Portland Roads - Preliminary Notes. Queensl. Govt, min. J., 37, pp. 336-338. (Iron Range mineral deposits.) SHEPHERD, S.R.L,, 1944. Wolfram on Banks Island, OueenBl. Govt, min, J., 45, pp. 209-214. SPENDER, M., I93O. Island-reefs of the Queensland Coast, Geogr. J., 76,pp. 193-214; 273-297; pis. 1-18, text figs. 1-9 2 maps. (Classification of roof debris according to formation Classification of reef islands according to height of reef) STANLEY, E.R., 1922, Report on the salient geological features and natural resources of the New Guinea Territory. 99 pp. maps, Melbourne. STANLEY, E.R., 1924. The Geology of Papua, Melbourne. 56 pp. map. STANLEY, G.A.V., 1928. Physiographic investigations in Queensland with reference to the Great Barrier Reef. Amer. J, Sei.. 16, pp.48-50. (Origin of Barrier Reef, based on physiography; Reefs N0 of Cairns regarded as pre- and during glacial and post-glacial; S, of this, post-glacial only.) SAINT-SMITH, E.C., 1918. Limestone at Ben Lomond, Bowen district. Queensl. Govt, min» ¿., 19 : pp. 559-560. SAINT-SMITH, E.C., 1919o Rock Phosphate deposits on Holbourne I., near Bowen, Queensl. Govt, min. J., 20, pp. 122-124. 349. STANLEY, G.A.V., 1928. The physiography of the Bowen district and of- the northern islands of the Cumberland Group (Whitsunday Passage)« Rent. Gt. Barrier Reef Cttee..2n.n. 1-51, text-figs.1-25. (Coastal geology; geology of coastal islands; emergence.) STEERS, J.A., 1929. The Queensland coast and the Great Barrier Reef. Geogr« J . , 74, pp. 232-257; 341-370; 15 pis.; 8 text-figs; 1 map. (Reef processes; geology of islands; geology of coastal he adland s; emer genee.) STEERS, J.A., 1930. A geographical introduction to the biological reports. Sei. Rents. Gt. Barrier Reef Exned., 3,pp* I-I5, 2 pis., 4 text-figs. STEERS, J.A., 1931. Evidences of recent movements of sea- level on the Queensland Coasts raised benches and the coral reef problem. C.R. Congr. internat. Geogr*, Paris, 1931, H , STEERS, J.A,, 1937. The coral islands and associated features of the Great Barrier Reef. Geogr* J.. 89, pp. 1-28, 119-146, 21 photos and 5 maps. (Reef processes; geology of islands; geology of headlands; emergence.) STEERS, J.A., 1938. Detailed notes on the islands surveyed and examined by the geographical expedition to the Great Barrier Reef in 1936, with appendix by H.G. Stubbings* Rent. Gt. Barrier Reef Cttee., 4, pp. 51-96, text-figs. (Reef island morphology and geology; reef processes.) STEPHENSON, T.A., STEPHENSON, G., TANDY, G. and SPENDER, M., 1931. The structure and ecology of Low Isles and other reefs, Sei. Rents. Gt. Barrier Reef Exned.. 1928-29, 3, pp. 17-112 27 pis., 15 text-figs. STUBBINGS, H.G., 1938. Marine sediments from Islands and Reefs of the Great Barrier Reef. Being appendix to paper by J.A. Steers. Rent. Gt. Barrier Reef Cttee.. 4, pp. 97-104. (Sedimentary petrography of reefs)• SUSSMILCH, C.A., 1938. The geomorphology of eastern Queens land. Rent. Gt. Barrier Reef. Cttee.. 4, pp. 105-134, pis. xii-xiv (Supposes continental shelf to be downfaultod block,) TAYLOR, T.G,, 1927. The Topography of Australia. Official Year Book Commonw. Austral., 20, pp. 75-86. 150 , TENISON-WOODS, J.E., 1881. Geology of northern Queensland. Trans. Qucensl. Phil. Soc.. 3> 16 pp. 189-238* VAUGHAN, T.W., 1917. Corals and formations of coral reefs. Ann. Rent. Smithson. Inst.. 1917. (Profiles through G.B.R., pp. 230, 231.) WALKQM, A.B., 1928. Fossil Plants from Plutoville, Cape York Peninsula. Proc. Linn. Soc. N.S.W.. 53 > PP* 145-150. WHITEHOUSE, F.W., 1947. A marine early Cretaceous fauna from Stanwell (Rockhampton District). Proc. roy. Soc. Queensl.. 57, pp. 7-20. WHITEHOUSE, F.W., 1955. The geology of the Queensland portion of the Great Australian Artesian Basin, pp. 1-20, Figs* 12, 17, 19, 32-^44, being Appendix G, to Report on Artesian Water Supplies in Queensland. Dept. Coordinator-General of Public Works, Queensland. WILKINSON, C.S., 1877. Notes on a collection of geological, specimens..... from the coasts of Now Guinea, Cape York and neighbouring islands. Proc. Linn. Soc. N.S.W.. I, pp.113-117.