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PART IL—GEOLOGY AND BOTANY.

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REPORT ON THE WORK

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Horn SCIENTIFIC EXPEDITION

CENTRAL AUSTRALIA.

ean lh GEOLOGY AND: BOTANY:

EDITED BY
BALDWIN SPENCER, M.A.,
PROFESSOR OF BIOLOGY IN THE UNIVERSITY OF MELBOURNE.

London
DULAU AND -CO., 37 SOHO SQUARE.

Melbourne
MELVILLE, MULLEN AND SLADE.

MARCH, 1896.

PRINTED BY
FORD AND SON, CARLTON,

MELBOURNE.

PART IIIl.—GEOLOGY AND BOTANY.

TABLE OF CONTENTS.

SECTION I.—PHYSICAL GEOGRAPHY AND GEOLOGY.

PAGE
PHYSICAL GEOGRAPHY By Professor Ratpu Tare and J. A. Warr,
M.A., B.Sc. = ss = - - - 1
GENERAL GEOLOGY -_ By Professor Raupu Tare and J. A. Warr,
M.A., B.Sc. (Plates 1 and 2) - - - 26
1. Previous Recorps AND REFERENCES ''t0 THE LITERATURE OF
THE REcion : 2 : : - : : = = 26
2. Pre-CAMBRIAN - - : : : = : * =) ys)
3. ORDOVICIAN © - = : = : 5 : : 3 : 46
4, Postr-ORDOVICIAN CONGLOMERATE — - = = : : = 60
5. Upper Creracrous 62
6. DeEsERT SANDSTONE (SUPRA-CRETACEOUS) - 65
7. Post-Crerackous PHENOMENA 68
8. TERTIARY ffl
ECONOMIC GEOLOGY - By J. A. Wart, M.A., B.Sc. 76
PETROLOGY : : - By W. F. Smeeru, M.A., A.R.S.M., and
J. A. Watt, M.A., B.Sc. (Plates 1, 2,3,4) 82
PALAMONTOLOGY — - - By Professor Ratpu Tare (Plates 1, 2,3) 97
SLCLLION I1,—BOTAN Y.
BOTANY - - - - by Professor Raupu Tare, with an Appen-
dix by J. H. Maipey, F.L.S. = =a
1. Tue LarapiIntine FLora : : : - z : - 117
2. Tue CEenrrRaAL EremMiAn F Lora : e = = : - 19]

APPENDIX. NovTES ON SOME VEGETABLE EXUDATIONS.
By J. H. Marven, F.LS. - : - - - - 195

Pinole ee HOGI AP ry.

BY PROPESSOR KALE SLATE tang Joa, WATT. 6.S¢

In dealing with the subject of the physical geography of Central Australia, it
is necessary to mention that only a very general and brief outline will be given, as

the space available does not permit of anything like a complete account.
It will be dealt with under the following heads :—

A.—MOUNTAINS.
1. McDonnell Ranges.
2. James, Waterhouse, George Gill and Levi Ranges.
3. Cretaceous table-topped hills, ete.
4. Ayers Rock and Mount Olga.
B.—RIVERS.
1. Finke Basin.
(a) Nature and position of its watersheds.
(6) Area of the Finke River Basin.
2. Finke River.
(a) Tributaries of the Finke.
(6) Length and rate of fall of the Finke channel.
(c) Nature of the course and channel of the Finke.
(27) Absence of surface running water,
(ec) Waterholes.
(f) Rainfall in its relation to surface waters.
C.—GORGES AND GAPS.
D.—LAKES.
E.—CLAYPANS.
F.—STONY PLAINS.

G.—SANDHILLS.

2 HORN EXPEDITION—PHYSICAL GEOGRAPHY.

A.—MOUNTAINS.

In the consideration of the physical geography of this country the mountain
system should first demand our attention, as being of primary importance, for on
it not only does the trend of the main valleys depend but also the size, number,
and even the very existence of the rivers, by reason of its influence on the wind
and rain. For the above reasons the McDonnell Ranges form the most important
physiographic feature of Central Australia. Were it not for the presence of this
chain of comparatively elevated land, with its important influence on the
meteorology of the surrounding country, the greater part of the interior would
resemble a sterile desert, which is the actual condition of portions of the stony and

sandy plains after a more than usually prolonged drought.

The most important mountain range within the area under consideration is
doubtless that of the McDonnell, which represents the much-denuded crest of one
of the highest folds, into which the crust of the earth within this area has been
thrown. In the crumpling of the earth’s crust the highest anticlines, being on the
lines of maximum disturbance, usually have cores of plutonic rocks. This seems
to have been the case with a great portion of the McDonnell Ranges, subsequent
movements having metamorphosed the originally plutonic rocks, thus causing

doubt as to their eruptive origin.

The mountain system of Central Australia does not consist alone of the
McDonnell Ranges and those immediately associated with them to the north and
north-east, as the Hart and Strangways Ranges, but includes also a number of
parallel ranges lying to the south, such as the James, Waterhouse, George Gill,
Levi, and Chandler Ranges, all representing the arches or troughs of the folds
produced by earth movements in past geological time. Examples of ranges occupy-
ing the troughs of the earth-folds are to be found in the case of the George Gill
and Levi Range. In each of these ranges, which really are portions of one and
the same range (their continuity being broken merely by the transverse valley of
Trickett Creek, a tributary of Petermann Creek, the latter a branch of the
Palmer), the rocks occupy a perfect synclinal trough, in which the sandstone dips
from the north and south towards the centre of the range at an angle of from
10° to 20°

The mountain system of Central Australia may be conveniently treated in
three divisions, the mountain ranges in each division for the most part comprising
rocks of one and the same geological age, while they differ from those of the other

divisions,

HORN EXPEDITION—PHYSICAL GEOGRAPHY. 3

Thus (1) the McDonnell Ranges proper, as well as the Hart Range, are
situated wholly, or nearly so, within the area occupied by metamorphic rocks of
presumably Pre-Cambrian age ; while (2), the James, Waterhouse, George Gill,
and Levi Ranges are wholly contained within the country occupied by Ordovician
strata ; and lastly (3), the low table-topped hills and groups of them, which one feels
disinclined to dignify with the name of mountains and mountain ranges, are entirely
formed of Cretaceous strata. Now, as each of these geological systems are repre-
sented by rocks differing in lithological character and structure, while they have
suffered differently from the dynamic forces of nature, the physical features of the
ranges occupied by strata of these different geological systems differ widely, and

will therefore be described separately.

(1) The McDonnell Ranges.

Dealing with the features of the most important first, we find that the
McDonnell Ranges trend in a nearly east and west direction for a distance of
about 400 miles, and have a width varying from twenty to fifty miles, thus

covering an area of more than 10,000 square miles.

In the meridan of Alice Springs Telegraph Station, which is situated from
three to four miles north of Heavitree Gap, where the River Todd breaks through
the southern boundary of the ranges under consideration, they have a width of

about twenty miles.

Westerly from this point they extend as a rugged main ridge, containing the
most elevated peaks, often capped by Ordovician quartzite, with a band of varying
width of “jumbly” hills flanking this main ridge on each side. About the longi-
tude of Mounts Liebig and Palmer (zc, about 131° 15’) the range becomes much

broken up.

Easterly from Alice Springs the range extends to about 136° east longitude ;
at 134° 10’ it becomes confluent with the south-east extension of Strangways
Range, with which it may be further considered to be linked by the Georgina
Range, about 134° 20’; while further east (about 135°) it is joined by Hart Range.
It may be said to extend approximately from the 130th to the 136th meridian
of east Jongitude, a distance of nearly 400 miles, and to le between 23° 7° and 23°

35’ south latitude, with an average width of between twenty to thirty miles.

These ranges have a very irregular outline, and have no parallel longitudinal
valleys; in fact, they present in no degree that uniformity of physical features
produced by earth movements and meteoric agencies, so familiar in the case of the

Ordovician ranges.
1A

4 HORN EXPEDITION—-PHYSICAL GEOGRAPHY.

The original stratification of the once sedimentary strata and the joints, that
were perhaps present in the original granites, have played to all appearances no
part in the moulding of the present physical features out of the metamorphic rocks,
the age of which is considered to be Pre-Cambrian. Rising abruptly out of the
elevated area of the McDonnell Ranges, with no linear arrangement, but irregu-
larly distributed, are a series of eminences, whose summits are in some cases, as in
that of Belt Range and Mount Sonder, capped by a northern extension of Ordovician
quartzite. To the presence of this protective covering, which has effectually
warded off the levelling forces of nature from the underlying less weather-resisting

metamorphic rocks, is probably due the comparative elevation of these peaks.

Ranged in order west to east the altitudes above sea level of the chief peaks
are as follows:—Mount Edward in Belt Range, 4649 feet ; Mount Heughlin,
4756 feet ; Mount Zeil, 4040 feet; Mount Sonder, 4496 feet ; and Mount Giles,
4210 feet.

The average elevation of the surrounding country is over 2000 feet above sea
level, so that these mountains are not so prominent as one might be inclined to
imagine judging alone from their altitude above sea level. They are nearly all
accessible, as the slopes are not usually very precipitous, except for example the
Belt Range (Fig. 3).

The movements of the earth’s crust, to which these ranges bear witness, were
to a great extent of Pre-Ordovician age, and were continued, though much
diminished in intensity, down to Post-Cretaceous times. During the earlier part
of the Ordovician period the Pre-Cambrian rocks probably underwent subsidence,
so as to allow of the deposition of Ordovician sediment that originally covered
much at least of the area now occupied by Pre-Cambrian rocks. Later they
partook of the Post-Ordovician upheaval, which converted much of the area
occupied by Ordovician sea into dry land. Later again this area has probably
participated in the gentle and gradual Post-Cretaceous upheaval, to which are

attributable the very slight undulations in the Desert Sandstone.

The extreme metamorphism of the Pre-Cambrian rocks is to a great degree
Pre-Ordovician ; but, as indicated by the gneissic character of much of the intrusive
granites, it was partly at least contemporaneous with that of the Ordovician
quartzites, etc. As should, perhaps, have been pointed out previously, the elevated
area occupied by the McDonnell Ranges forms a great part of the northern
boundary of the Lake Eyre Basin. In travelling southwards from this elevated

region towards the centre of the basin, we descend by means of a series of terraces

HORN EXPEDITION—PHYSICAL GEOGRAPHY. 5

formed by the Ordovician ranges, each one on a lower level than its predecessor on
the north, on to wide and extensive plains occupied by Cretaceous rocks and by

stony and loamy plains and sandhills.

These last features have been formed from the déé77s derived partly from the
Cretaceous strata, which d@édr7s has been accumulating through the Late-Tertiary
and Post-Tertiary epochs, and is still accumulating at the present day. Such
plains, near their northern limit at Jeast, are not less than 1000 feet above sea
level. Still they slope so gently to the south towards the centre of the basin, “e.,
towards Lake Eyre, that their elevation above sea level is no index to their altitude
above the surrounding country. The streams which have eroded them have not
generally excavated their channels deeper than from 200 to 250 feet below the

original surface of the country.

(2) The James, Waterhouse, George Gill and Levi Ranges.

The next division of the mountain system includes the ranges situated within
the Ordovician area. Beginning from the north these comprise the quartzite ridge
which forms the southern boundary of the Pre-Cambrian area, and in which are
the Heavitree, Emily, Temple Bar, ete., Gaps. This ridge is succeeded on the
south by the Waterhouse, James, George Gill, Levi and Chandler Ranges. These
ranges consist of a series of parallel ridges of quartzite and sandstone, with a nearly
east and west trend, separated by numerous parallel and often very persistent and
regular longitudinal valleys. These valleys are generally very narrow, often less
than a mile wide, but sometimes open out, as in the case of the Missionary Plain,

to a width of from twelve to fifteen miles.

Intersecting these ranges are numerous short transverse valleys, frequently
entirely occupied by the channels of the creeks, which have eroded them. One of
these creeks often extends for long distances along one of the longitudinal valleys,
and then suddenly bursts through the range through a narrow gorge, to resume its
course along a second longitudinal valley at a lower level than the first, and perhaps
to pass through a second gorge in its passage towards Lake Eyre. These ranges
extend easterly, as far at least as those of the previous division have been traced,

while westerly they practically terminate at 151° 20° (about) east longitude.

They have a mean combined width, if we include the intervening plains and
valleys, of from sixty to seventy miles. The area occupied by them, therefore,
must be more than 15,000 square miles. The highest points are situated in the

most northern ridge, as in the case of Mount Gillen, which must be nearly 3000

6 HORN EXPEDITION—PHYSICAL GEOGRAPHY.

feet above sea level. The mean elevation of this ridge is about 2500 feet above
sea level, that of the Waterhouse Range about 2200 feet, that of the James Range
about 2000 feet, while lastly the mean elevation of Chandler Range is only about
1500 to 1600 feet. From these figures it can be clearly seen that there is a gradual
decrease in elevation in the ranges from north to south, each range to the south
constituting, as it were, a step in the descent from the McDonnell Ranges to the

plains.

The chief factors, in addition to the position of the longitudinal valleys
occupying the original troughs of the folds, that have influenced the direction of
the lines of denudation are (1) the lines of weakness on the crowns of the anticlinal
arches, and (2) the position of the bands of limestone. An example of the
influence of (1) is furnished by the valley of Petermann Creek, which has been
eroded out of an anticlinal arch, while the rocks of the corresponding synclinal
trough now form the George Gill and Levi Ranges. The influence of (2), as might
have been expected, is to be observed throughout this region, the greater number
of the valleys within these ranges having been, to a great extent, eroded out of the

limestone beds.

The angle of inclination of the mountain slopes depends to a great extent on
the nature of the strata and on their dip. On one side of the ridge the slope
often conforms to the dip of the strata when these are inclined at fairly steep
angles. On the south side of the quartzite ridge, for instance, which forms the
northern boundary of this area, the inclination of the strata (quartzite and lime-

stone), as well as that of the mountain slope, is from 60° to 70°.

The north face,of this ridge, however, presents for almost the total thickness
of the quartzite a sheer perpendicular escarpment extending from the summit
downwards 200 or 300 feet. Below this quartzite, as at Mount Gillen, the
remaining 600 to 700 feet of this face, composed of Pre-Cambrian gneiss, has a
slope not exceeding 30° to 40°. A similar difference in the inclination of the
slopes of a ridge is also to be seen in the case of the Mereenie Escarpment, which
probably extends almost continuously as far east as the Finke River. On the
north side there is a steep, almost perpendicular, escarpment from 500 to 600 feet

high, whereas on the south the slope conforms to the dip of the strata.

In those ranges, where the sandstone is dipping at very low angles, as in the
George Gill and Levi Ranges, we find very steep, almost vertical, escarpments on
both sides. The northern face of Levi Range, for instance, rises to an elevation

of about 500 feet above the valley of Petermann Creek, for nearly 300 feet of

HORN EXPEDITION—PHYSICAL GEOGRAPHY. 7

which it is almost vertical. At the foot of this escarpmont there is a talus slope

nearly 200 feet high, with an inclination of about 30°,

(3) Cretaceous Table-topped Hills and Table-lands.

Although there are no mountains or mountain ranges worthy of the name
within the Cretaceous division, the altitude of the Cretaceous plains near the
northern limit of this area is as much as 1000 feet above sea level. These
elevated plains slope gradually towards Lake Eyre from an altitude of 1000 feet

above sea level to thirty-nine feet below sea level at Lake Eyre.

Rising out of these plains are numerous table-topped hills and low flat ranges
and table-lands, isolated from one another by denudation, Some of the highest of
these rise to an altitude of from 300 to 400 feet above the surrounding plains, and
thus in the northern part of this Cretaceous area to 1200 to 1300 feet above sea
level. These isolated masses are separated by “stony ” and “loamy” plains and

)

“sandhills.” The hills are usually crowned by a layer a few feet in thickness of
an exceedingly hard rock, representing sometimes a sandstone, sometimes a grit,
and at other times a finer-grained and more argillaceous rock. Between the grains
of this rock hydrated silica has been deposited from solution. To the presence of
this cement is to be attributed its extreme hardness and often more or less
conchoidal fracture. This so-called “desert sandstone,” or porcellanite, when
finer-grained and more argillaceous, protects the under-lying strata from denuda-
tion in a way that may be compared to the protective action of the boulders in the

case of the famous earth-pillars of certain villages in the Tyrol.

Chambers Pillar, for instance, a well-known feature situated ten miles north
of the old Idracowra cattle station on the Finke, might be likened to an earth
pillar, the indurated ferruginous sandstone of its summit taking the place of the
boulder of the earth-pillar, and protecting the sandstone of the pillar from removal
by denudation. The isolation of Chambers Pillar, for it is surrounded on all sides
by red sandhills, is probably due to the purely local character of the indurating
process, or rather perhaps to the induration having been more intense in the
locality of the Pillar, than in the once surrounding rock, now entirely denuded.
The Pillar, if we include in this term the whole structure from base to summit, is
divisible into two parts—a basal portion or pedestal 500 yards in circumference at
its base and 100 feet high, and a column surmounting it, sixty-seven feet high and
eighty yards in circumference at its base. The whole, with the exception of the

few feet of more indurated rock on its summit, consists of a yellow and white

8 HORN EXPEDITION—PHYSICAL GEOGRAPHY.

friable sandstone slightly tinged yellowish-red externally by hydrated ferric oxide.
The presence of this layer of indurated rock explains the fact that the isolated
Cretaceous table-topped hills have usually the form of truncated cones, the topmost
stratum generally presenting a vertical edge for its whole thickness, while the
slope of the portion of the hill occupied by the underlying softer strata varies from
32° to 40° from the horizontal.

(4) Ayers Rock and Mount Olga.

In addition to the foregoing mountain ranges there are some _ isolated
mountains within the area examined that require a brief description. Rising like
an enormous water-worn boulder, half buried in the surrounding sea of sandhills,
is that remarkable isolated monolith known as Ayers Rock. It is situated about
thirty-two miles 8.8.W. of Lake Amadeus. The summit of this monarch of the
desert can be seen from a distance of more than forty miles. At a nearer view its
smooth, bold, flattened, dome-like outline stands out clear and distinct. This inter-
esting relic of an ancient geological formation has puzzled explorers in no small
degree. It rises to an elevation of about 1100 feet above the surrounding plains,
and about 2500 feet above sea level. The sides of the rock, which has a circum-
ference at its base of nearly five miles, are very steep, almost vertical in places and
practically inaccessible, although Mr. Gosse succeeded after great trouble in
ascending it. The rock is quite bare, with the exception of a few fig-trees, which

maintain a precarious footing in the few crevices on its bare sides.

The rock has been often mistaken for granite, to which it bears some super-
ficial resemblance, both in its lithological aspect and in its mode of weathering.
The original sedimentary character of it, however, is unmistakeable, numerous
very small rounded pebbles of quartz and felspar being distinctly visible in hand
specimens. Although once a sedimentary rock, it has been to some extent altered
by metamorphic agencies, a small amount of mica, perhaps of secondary origin,
having been formed. The rock is a very indurated, and to some extent altered,

arkose sandstone, decidedly gritty in parts.

The sides of this rock ascend in places quite vertically for a distance of 500
to 600 feet, while some of the more sloping faces are marked by a series of terraced
waterfalls rising one above the other. A peculiar netted appearance is to be seen
on some of the faces, a good example being visible on the northern face. This is
due to the irregular weathering of the rock, the softer spaces, which have disap-

peared, having been separated by small intersecting veins of a harder material,

HORN EXPEDITION—PHYSICAL GEOGRAPITY. 9

perhaps due to segregation along certain lines, which now stand out as low

reticulate ridges.

A noteworthy feature of the rock is the manner in which it peels off. Firstly,
on a small seale, thin flat flakes an inch or two in diameter and from one-eighth
to a quarter of an inch in thickness are seen to be separating from the rock in all
directions, and along no definite plane or set of planes. Secondly, on a large scale
there may be seen, sometimes leaning against the base of the rock, having slipped
from « higher level, or lying round its base, immense blocks of rock which have
peeled off from the mountain, the phenomenon resembling on a large scale the
concentric weathering of many eruptive rocks. In one or two places large blocks
can be seen detached sufticiently to allow the sunlight to pass between them and
the main mass, but still not entirely separated. One of these measures 8’ x 5’ x
200’, while others which are leaning against the base of the rock measure 6’ x 5’

20’ and 12’ x 6’ x 60’, Caves, usually of a small size, occur both near the
base and on the sides and slopes of the rock. Lastly, a ridging is observable,
which probably indicates the direction of foliatjon planes, trending in a N.W. and
S.E. direction.

Fifteen miles west of Ayers Rock is another remarkable mountain mass, the
most prominent and elevated portion of which is called Mount Olga. This, with
numerous other peaks which rise from a common base, forms an isolated mass
surrounded by red sandhills. Mount Olga rises to an elevation of about 1500 feet
above the plain, and over 3000 feet above sea level. It appears to be composed of
a coarse conglomerate from top to bottom, which consists for the most part of
pebbles of granite and other eruptive rocks. The southern face of this mass is
about five miles in length, and its western extremity rises perpendicularly for

nearly 1500 feet.

Mount Olga from a distance presents a most remarkable outline, the many
rounded dome-like elevations reminding one of the features usually presented by

granite ranges.

B.—RIVERS.

The country traversed by the Expedition between Oodnadatta and the
McDonnell Ranges lies wholly within a region of internal drainage, divisible into
two basins, the centre of the largest and most important being Lake Eyre, and
that of the other being Lake Amadeus. The basins of Lakes Eyre and Amadeus

will be described in detail later. We will in the meantime contine our attention

9

10 HORN EXPEDITION—PHYSICAL GEOGRAPHY.

to that portion of the Lake Eyre Basin, which is drained by the Finke, one of the

most important rivers of the interior of Australia.

The McDonnell Ranges and the eastern extension of the Hart Range may be
said to divide the drainage of the interior into two areas, of which the southern,
which forms part of the Lake Eyre Basin, contains the most important rivers.
The Finke, with its large tributary, the Hugh, takes its rise on the southern slope
of these ranges, and flows towards Lake Eyre in a general southerly to south-
easterly direction. The majority of the small creeks, which issue from the northern
slope, do not discharge their waters into any common basin, but each maintains
an independent course for a longer or shorter distance from the ranges, to become
sooner or later absorbed by the sandhills and loamy plains. These latter creeks,
of which the Darwent, Dashwood, Charley, Six Mile, Muller, etc., are examples,
leave the ranges and flow northwards over the surface of the elevated plain, which

is known to the north of Alice Springs as Burt Plain.

They have dry sandy channels, the banks of which are lined with gums,
which are numerous and of vigorous growth near the ranges. There are a few
creeks of this character heading from the south-western extremity of George Gill
Range, e.g. King and Laurie Creeks. The former of these flows southwards in
the direction of Lake Amadeus, but the flow of the water at fifteen or twenty
miles from its source is not strong enough to form a channel, with the result that
the flood waters spreading out over wide “gum flats” become absorbed by the

surrounding sandhills.

There are, in addition to the above-mentioned small creeks, two or three larger
ones taking their rise on the north slope of the McDonnell and Hart Ranges near
their eastern extremities, which after a short northerly course sweep round to the
south and flow towards Lake Eyre. As an example of these may be mentioned
the Hale, the Sandover, and the Plenty, the two last of which ultimately unite to
form the Marshall or Hay River. Speaking generally, one may say that the
drainage from the southern slope of the McDonnell Ranges and from those ranges
lying immediately to the south is sooner or later collected into one main channel
known as the Finke, which trends in a general south-easterly direction towards

Lake Eyre.

(1) Finke Basin.

(a) Nature and Position of its Watershed.—The northern limit of the Finke

Basin is to a great extent formed by the McDonnell Ranges, the line of water-

HORN EXPEDI'TION—PHYSICAL GEOGRAPHY. ll

parting extending along the northern edge of these ranges. The water-parting

does not, therefore, traverse what are now the most elevated points in the ranges,
such as Mounts Gillen, Sonder, ete., but les wholly to the north of the ridge
containing these points. This fact probably indicates that the summit of the arch,
which originally determined the line of water-parting, lay near the northern edge

of the McDonnell Ranges.

The mean elevation of the northern watershed is nearly 3000 feet above sea
level. The water-parting of the Finke Basin runs along the northern edge of the
McDonnell Ranges westerly to about Mount Zicl From this point a straight
line to the north-western extremity of Gardiner Range would nearly represent
the north-west boundary of the basin. The western line of water-parting extends
from this latter point to George Gill Range, and thence E.S.E. along the southern
face of Levi Range. From Levi Range the rest of the western watershed is not
well known; it passes at all events through the eastern extremity of the
Musgrave and Everard Ranges. The exact eastern limit of the basin is practically

unknown.

(6) Area of the Finke River Basin.—The area of the Finke River Basin
rannot be less than 80,000 square miles. The basin is roughly triangular in
shape, with the apex situated at Lake Eyre and the base coincident with the
northern water-parting. The northern portion of the basin is the most elevated,
the drainage being to the south and south-east. The mean elevation of this
northern portion cannot be less than from 2500 to 3000 feet above sea level.
About half the way between the northern watershed and the apex of the basin the
mean elevation is about 1000 feet, while at Lake Eyre itself is is a few feet below
sea level. A rough calculation of the average elevation of the basin makes it at

least 800 feet above sea level.

(2) The Finke River.

(a) Tributaries of the Finke—On the north side of Finke Gorge, through
which the Finke flows in its southerly course, this river is formed by the junction
of two creeks. The eastern branch, known as Ormiston Creek, rises on the
northern edge of the McDonnell Ranges, and bursts through the prominent
quartzite ridge between Mounts Giles and Sonder. The western branch, the
Davenport, which is the more important of the two, takes its rise two to three
miles S.E. of Mount Ziel, and flows for a few miles to the south, where it is
known as the Crawford. It then suddenly turns to the east and is known as the

Davenport. Before, however, it junctions with Ormiston Creek it is joined by
2A

12 HORN EXPEDITION—-PHYSICAL GEOGRAPHY.

several small creeks, notably Redbank and Rockybar Creeks, both of which take
their rise in the northern portion of the McDonnell Ranges, and, going south,
force their way through narrow gorges in these ranges. The Finke flows south-
wards from the junction of Ormiston Creek and the Davenport, and at twelve
miles from that junction, measured in a direct line, it is joined on the west by
Rudall Creek, which rises in the south-western extremity of the south McDonnell

Range, about 132° BE. longitude, and which flows almost due east to the Finke.

Bending more towards the east, the Finke flows past the Mission Station
(Hermannsburg), entering the Krichauff Range one mile south of this point.
After a meandering course of from ten to fifteen miles through this range in a
general §.8.E. direction, it is joined on the east by an important tributary, known
as Ellery Creek. This latter takes its rise on the northern edge of the
McDonnell Ranges, about 132° 50’ E. longitude, and flowing 8.8.W., forces a
passage through two quartzite ridges on its way to join the Finke. On its exit
from the Krichauff and James Ranges, the Finke is joined on the west by Ipilla

Creek, a small tributary having its source in the James Range.

From this point the general course of the river is 8.E. and is extremely
tortuous. When it reaches 24° 45’ S. latitude and 133° 22’ E. longitude it is
joined on the west by a very important tributary, the Palmer. The Palmer takes
its rise on the northern slope of the James Range, about 132° E. longitude and
23° 4U'S. latitude., and flows in a general 8.E. direction through this range for
sixty miles, when it is joined on the west by an equally important tributary, the
Walker. This latter has its source in the north-western extremity of Gardiner
Range, and flows with a general E.S.E. course. The united streams, known as
the Palmer, flow in an E.S.E. direction to junction with the Finke, 100 miles from
the point where the Walker junctioned with the Palmer.

Petermann Creek, of less importance than the above-mentioned tributaries,
takes its risein what is known as Petermann Pound, a plain nearly five miles in
diameter encircled by a line of hills about 400 to 500 feet high. This semicircle
of hills unites George Gill Range with a western extension of that portion of the
James Range known as the Station Range. From the Petermann Pound, Peter-
mann Creek flows about due east, and occupies a longitudinal valley between
George Gill and Levi Ranges on the south and a portion of the James Range on
the north. In its passage eastwards it is joined by numerous small creeks flowing
from the ranges on each side, one of the largest being Trickett Creek, which takes

its rise on the south-east face of George Gill Range, and flows N.K. The valley of

HORN EXPEDITION——PHYSICAL GEOGRAPHY. 13

Trickett Creek separates George Gill Range from Levi Range, which would

otherwise constitute one continuous range.

Petermann Creek, after a nearly easterly course of about forty-five miles, joins
the Palmer at ten or twelve miles below the Walker junction, From the Petermann
junction the Finke pursues a nearly E.S.E. course for sixty miles, when it is joined
by a very important branch, the Hugh. This river has its source on the northern
edge of the McDonnell Ranges, about twenty-five miles west of Alice Springs, and
sweeping through the range at Brinkley Bluff flows in a general E.S.E. direction.
The Finke is next joined on the west by the Lilla at a point thirty-two miles in a
direct line 8.S.E. from the Hugh junction. About thirty-six miles in a direct S.E.
line from the last point another creek, the Goyder, joins the Finke on the west.

Further south still, and to the east of Charlotte Waters, it is joined by the Coglin,

Below the junction of this creek the Finke has no detined channel, but spreads
out over wide alluvial flats. Sixteen miles S.S.E. of Charlotte Waters the tele-
graph line crosses Adininga Creek, which runs easterly to the flats over which the
Finke waters spread. Still further to the south the Alberga, which takes its rise
in the eastern extremity of the Musgrave Range, after being joined on the north
by a tributary, the Stevenson, and being then known as the Macumba, flows
E.S.E. towards Lake Eyre. It is into the Macumba that part of the flood waters
of the Finke flow on their way to Lake Eyre. The greater portion, however,
disappears from the surface, and is absorbed by the vastly extensive sandhills and
plains, which stretch round the north and east sides of Lake Eyre. In the above
description of the Finke and such of its tributaries as occur in the area examined
by the Expedition, no mention has been made of the Todd, an important stream
which takes its rise on the northern edge of the McDonnell Ranges to the north
of Alice Springs. It leaves these ranges at Heavitree Gap, and at first has for
many miles an easterly course, after which it turns 8.8.E. towards Lake Eyre. It
is very probable, but this is not certainly known, that the Todd junctions with the

Finke south of Charlotte Waters.

(6) Length and Rate of Fall of Finke Channel.—The total length of the Finke
from its source in the McDonnell Ranges to Lake Eyre must be about 1000 miles,
although the distance in a direct line is not greater than 500 miles. A few caleu-
lations have been made on the rate of fall of the channel of the Finke over
different portions of its course. The difference in the altitudes above sea level of
the channel of the Finke at Mount Sonder and at the Mission Station, a distance

of fifty-four miles, is about 490 feet. These data give a rate of fall of about nine

14 HORN EXPEDITION—PHYSICAL GEOGRAPHY.

feet per mile. Between the Mission Station and the junction of the Palmer with
the Finke the rate of fall is five feet per mile, the difference in the altitude of the
two places being 699 feet, and the distance between them 135 miles. Lastly, the
difference in the altitudes of the Finke Channel at’ the Palmer junction and at
Lake Eyre, a distance of 536 miles, is 980 feet, which gives a mean rate of fall of
less than two feet per mile. Between Heavitree Gap (1713 feet above sea level)
and Oodnadatta (397 feet above sea level), a total distance in a direct line of 357

miles, the fall of the slope of the surface averages about 3°7 feet per mile.

The above figures show, as might have been expected, that the rate of fall is
at its maximum in the McDonnell Ranges, and at a minimum on the Cretaceous
plains near Lake Eyre, between which places there is a gradual decrease in the

rate of fall as we go from north to south.

(c) Mature of the Course and Channel of the Finke.—As one might expect,
judging from the figures just given, the course of the Finke from the McDonnell
tanges to the southern slope of the James Range is not so sinuous as it is after
it debouches upon the Cretaceous plains. On these plains its course becomes
extremely meandering, the river making its way down the very gentle incline
from these ranges to Lake Eyre only after performing numerous sweeping curves.
The width of its channel varies considerably, being usually narrower and deeper
in the ranges, but widening out as it leaves them. On emerging on to the plains
it becomes flatter and shallower and dotted with gum trees, which are not confined
to the banks only as in the ranges, but grow often in patches eyen in the middle

of the channel.

(2) Absence of Surface Running Water.—The absolute dependence of the
presence of running water in the bed of the Finke upon direct supplies of rain has

its explanation in the following facts :—

(1) The basin of the Finke, although of great extent, is entirely confined, or
nearly so, to an area over which the climatic conditions are the same.

(2) Rain falls usually only at certain seasons, there being long intervals of
drought.

(3) There is an almost total absence of springs at the head of the Finke and
its tributaries, and in the few instances of their occurrence the discharge is very
small,

The influence of these three factors on the absence of surface running water

is obvious. After the flood waters caused by a heavy downpour have subsided,

HORN EXPEDITION—PIYSICAL GROGRAPITIY. 15

and during the long intervals of dry weather, surface running water is absent from
the greater length of the channel, its appearance for short distances only at certain
parts being due purely to local causes. The absence or paucity of springs is to be
attributed to the absence of a sufficiently thick layer of soil on the mountain slopes
to act as a reservoir by absorbing the rain water and giving it out gradually at
lower levels in the form of springs. It is also due to the absence of joints in the
Pre-Cambrian and their searcity even in the Ordovician rocks. The rain waters
are, therefore, not absorbed, but form torrents, and rush down the bare mountain
slopes into the valleys. When the waters have reached the beds of the water-
courses, their rapid absorption by the porous strata and the excessive amount of
evaporation that is always taking place cause the almost total disappearance of

surface water from the river channels.

(e) Waterholes.—At certain seasons of the year, should the fall of rain be
sufficiently great, the supply of water in the channels of the rivers exceeds the
amount that can be absorbed by their sandy beds, and this produces a flow of water
down the channel. This is often spoken of locally as a flood, as the waters as a
rule are not confined to the channel by the low river-banks, but spread out over

the wide alluvial flats which border the main channel.

When rain ceases to fall the flow of water diminishes almost immediately in
volume. This it continues to do until running water disappears from the surface
over an ever-increasing leneth of its course. There are, however, for a month or
two after a heavy rainfall portions of the channel over which running water may
still be seen; but these gradually decrease in length until the channel assumes
what may be termed its normal state. In this state the channel is oceupied by
long stretches of white sand devoid of surface water, separated at rare intervals by
short lengths of the channel, where water may be seen flowing gently over a rocky
bed. In the apparently waterless stretches, however, water may be obtained by
sinking to depths varying with the nature of the bottom and the lapse of time
since the last heavy fall of rain. The appearance of surface water at rare intervals
in the bed of the river is due to the presence of “bars” of rock, which cross the

channel at these places.

As the water in its downward progress cannot filter through these rocks as it
does through the sand and gravel at other parts, it has to rise to the surface to
pass over them. The change from the normal state of the channels to their next
condition is a more gradual one. As the supply of water becomes less and less,
the amount and rate of flow over the rocky bars gradually diminish, until finally

the supply becomes too small to cause the water to rise over them at all.

16 HORN EXPEDITION—PHYSICAL GEOGRAPHY. ‘

When the river has reached this stage in its desiccation, the isolated and
often widely-separated waterholes and rockholes become economically important
features. The principal waterholes occurring in the beds of the rivers and creeks

may be described under the three following headings :—

1. Rockholes confined to gaps and gorges.

bo

. Waterholes on the upper sides of bars of rock.

Co

. Waterholes not associated with rocky bars, but occurring in the rivers

where the bed is impervious.

1. Rockholes confined to Gaps and Gorges.—These occur in the many gaps
and gorges through which the rivers and creeks have forced their way in their
southerly course from one longitudinal valley to the next. In the quartzite ridge,
for instance, forming the southern boundary of the south McDonnell Ranges
proper, there are many gaps, the beds of the rivers in these being partly occupied
by pools of usually excellent water. Such waterholes occur in the Redbank,

Finke and Ellery Creek Gorges, and in Simpson and Emily Gaps.

The great strength of the current of the water flowing through these gaps,
due to the fact of the streams being confined within narrow bounds, sweeps all
detritus out of them and erodes the river bed to a greater extent here than else-
where, thus often producing deep rockpools which retain large quantities of water.
Many of these rockholes, owing to their sheltered positions, are practically

permanent.

2. Waterholes on the Upper Sides of Bars of Rock.—The second class of water-
holes are those situated on the upper side of some rocky bars. Jf the flow of
water over the portions of the river channels in which these occur is strong, then
the eddy in front of the bar causes the removal of sand and gravel from this side,
and leaves, as the water subsides, a depression filled with water. Unfortunately,
however, at a later period a light rain often causes a flow of water just strong
enough to carry sand, etc., into this hollow and thus obliterate it. For this and
other reasons one cannot always depend upon getting water on the surface at these
places, even though one may have seen on a former occasion a fine pool of water at
the same place, A very good example of this class of waterholes occurs in the
Finke near Henbury Cattle Station.

3. Waterholes not Associated with Rocky Bars.—The third class of waterholes
owe their existence to their being situated over the portions of the river beds where

fine silt or mud takes the place of porous sand and gravel, and thus prevents the

HORN EXPEDITION—-PHYSICAL GEOGRAPHY. , 17

percolation of the water below the surface. When the flood-waters abate over these
portions, there usually remain a string of waterholes occupying the depressions in
the river bed. If rain does not fall for some time these one after another lose
their water by evaporation and become dry. Only those which occupy the deepest
and most sheltered depressions hold out for any length of time. Such waterholes
prevail in the Cretaceous area as in the Stevenson, Macumba and Coglin Rivers,

and form the chief sources of supply in the districts where they occur.

What a valuable provision of nature in reality are the sandy beds of the
rivers! Through the sand and gravel the water creeps slowly down its course
protected toa great extent from evaporation, and here it may generally be obtained
by sinking ; whereas if it had remained on the surface it would have been rapidly
evaporated. Only in those places where ledges of rock cross the channel do the
waters appear at the surface, and then usually for a short distance only, disappear-

ing again in the sand on the other side of the rocky bars,

Seldom do the flood-waters of the Finke and Macumba flow over the surface
to Lake Eyre; for the lacustrine delta of these rivers, consisting for the greater
part of deposits of sand and loam which have been accumulating during the Late-
Tertiary and Post-Tertiary epochs absorb the immense body of water brought
down by these rivers.

(f) Rainfall in tts Relation to Surface Water.—The rainfall throughout the
area of the Finke Basin is somewhat variable, ranging from an average of less
than five inches per year in the central and southern portions to ten or twelve
inches over much of the mountainous country in the northern part of the basin.
The mean annual rainfall throughout the basin cannot be more than six to seven

inches.

A great part of the moisture that falls as rain throughout this area is lost by
evaporation. From claypans and all shallow depressions which expose large
surfaces to the desiccating agents, the water disappears in two or three months
after a fall of rain. From the waterholes, too, during the dry season the water
disappears at an alarming rate. Waterholes which have been examined by one
explorer during a good season, and declared to be permanent, have, when examined
later by a second explorer in a rather dry season, been often found to be dry or
nearly so, Explorers have indeed been rather too hasty in forming conclusions as
to the permanency of waterholes, which, visited perhaps during a good season,
contained a good supply of water, but which had in reality no element of
permanency. In the great majority of cases they are not fed by springs nor

situated in places sufliciently sheltered to give practical permanency to them.

2
3

18 HORN EXPEDITION—PHYSICAL GEOGRAPHY.

Besides the great quantity of water directly evaporated, some of it goes to
supply the wants of the Gums which line the banks of the creeks. In times of
heavy flood some of the water may reach Lake Eyre along the channel of the
Macumba, while a large portion filters gradually down towards Lake Eyre through
the bed of the creek at a moderate depth from the surface. Lastly, an important
portion of the rainfall percolates through the outcrops of the porous strata of
Cretaceous age, travels downwards towards Lake Eyre, and forms the supply from
which the artesian water is derived. Some of this water reaches the surface again
in several localities by natural outlets, and issues from the mouths of mound
springs. Some of the water probably percolates through the sand and gravel of
the river beds, and in this way reaches the water-bearing strata of the artesian
basin.

C.—GORGES AND GAPS.

The next features to be described are the gorges and gaps, which are rather
numerous in the ranges in the northern portion of the region under consideration,
and through which many of the rivers flow on their ways southwards towards Lake
Eyre. These features are in the form of narrow rocky passes with walls usually
of quartzite, but sometimes of sandstone, rising almost vertically to heights varying
from 200 to 700 or 800 feet above the valleys. Their length varies exceedingly,
while in width they range from a few feet to forty or fifty yards. Many of the
rivers after flowing equatorially for some distance along the longitudinal valleys

turn abruptly to the south, and cross the ranges through these gaps.

In most of the gaps are beautiful pools of clear fresh water, in which large
numbers of fish live, belonging, however, to a few species only. It has been
thought that these gaps occupy the sites of faults in the strata, but it appears to
us to be quite unnecessary to call in the aid of such dislocations to account for
their origin. The origin of the majority of the gaps is probably due to the erosion
of the river beds in the positions of the present gaps keeping pace with the upheaval
and folding of the strata in those places. By thus lowering their channels the
rivers have maintained their original positions. In a few cases, however, the
gorges may owe their existence directly to faults, the water readily eroding a

passage for itself along the fault planes and their associated cracks.

D.—LAKES.

The interior district of Australia, 7e., the portion which has an internal

drainage, comprises an area of nearly a million and a half square miles, and is,

HORN EXPEDITION—PHYSICAL GEOGRAPHY. 19

therefore, seven times as large as the Great Basin of North America. It will
thus be readily understood that the lakes, which form the centres of the several
drainage basins, are physical features of the greatest interest and importance.
Surrounding the area of internal drainage is a strip of country stretching inland
from the coast for varying distances, throughout which the rivers carry the surface

water to the ocean.

Only two lakes occur in the region considered in this paper, viz., Lakes Eyre
and Amadeus, each of which forms the centre of one of the divisions of the internal
basin. Both of these are fast passing into the state of dry basins. This is due in
the first place to the aridity of the climate throughout the region occupied by
them, from which results an almost total absence of superficial flow of water into
the lakes, especially Lake Amadeus; and in the second place it is due to the

accumulation in the lakes of sand, ete., transported thither by running water or

s
wind. These statements apply in a special manner to Lake Amadeus, the absence
of surface water near its western extremity at any rate being specially noticed by

Mr. Tietkens.

From the sandhills bordering the lake near Gosse’s Crossing, /.e., towards its
eastern extremity, we could make out no water on its surface. There the dry bed

of the lake was crossed without trouble ex route to Ayers Rock and Mount Olga.

Of these two lakes Eyre is the larger and the more important, and will be

considered first.

Lake Eyre.

Lake Eyre receives the drainage from the McDonnell Ranges, and the ranges
lying immediately to the south of them, together with the drainage from a great
part of west and south-west Queensland, Its basin includes those of all the rivers
that drain into it, and having no outlet it is entirely encircled by a line of water-
parting. The drainage throughout the basin is to the 8.H., 5., and 8.W., Lake

Eyre itself being situated close to the southern border of the basin.

The Lake Eyre Basin occupies the eastern half of South Australia between
the northern termination of Flinders Range and the McDonnell Ranges, and
the greater portion of west and south-west Queensland from the Great Dividing
Range westwards. The rivers which drain this enormous area are taken in order
from west to east, the Neales, Macumba, Finke, Todd, Hale, Sandover, Plenty,

Mulligan, Diainentina, and Cooper or Barcoo,
3A

20 HORN EXPEDITION—PHYSICAL GEOGRAPHY.

The western boundary of the Lake Eyre Basin is formed by the Cretaceous
plains flanking on the east the Everard Range, in which the Neales River takes
its rise, by the eastern extremity of the Musgrave Range, from which the Alberga
heads, and by the western extremities of the George Gill and Gardiner Ranges,
where some of the large tributaries of the Finke have their sources. The northern
boundary is formed by the McDonnell and Hart Ranges. The north-eastern and
the eastern are formed by the Selwyn, McKinlay, and the Great Dividing Ranges,
in which the sources of the Mulligan, Diamentina, and Barcoo (Cooper’s Creek)
are situated. Lastly, the southern boundary is for the most part formed by the
northern slope of the Flinders Range, from which short narrow creeks flow north-
wards to Lake Eyre.

Form, Area, etc.—The general form of the basin is roughly quadrilateral,
with one angle situated on the northern slope of Flinders Range, to the south of
Lake Eyre south. Another of the angles coincides with the western extremity of
the McDonnell Ranges about Mount Ziel. A third lies near the head of the
Mulligan and the last is situated about the source of the Barcoo River. The
total area of the basin cannot be less than 500,000 square miles, the greatest
breadth, lying along the 24th parallel, is about 900 miles, and the greatest
length, occurring about the 137th meridian of E. longitude, is about 750 miles.

Lake Eyre itself, including Lake Eyre south, lies within the 137th and the
138th meridians of EK. longitude and between 27° 50’ and 29° 29'S. latitude, and
occupies an area of about 5000 square miles. It is situated almost at the very
southern extremity of the basin, the south edge of Lake Eyre south being only a
few miles north of the northern extremity of Flinders Range. The margin of

Lake Eyre has been calculated to be thirty-nine feet below sea level.

Lake Amadeus.

The Lake Amadeus Basin is not well known, but it appears to be of small
extent as compared with that of Lake Eyre. It comprises in all probability an
area of between 20,000 and 30,000 square miles. The northern boundary of the
basin extends probably from the western end of George Gill Range to Watson
Range, and thence along the north of the 24th parallel to about the Western
Australian border. The southern limit of the basin lies possibly along the
Rawlinson and Petermann Ranges, while its eastern and western boundaries are

apparently unknown.

HORN EXPEDITION—PHYSICAL GEOGRAPHY. 21

Lake Amadeus itself was discovered and named by Mr. Ernest Giles in 1872,
when it proved an insuperable obstacle to him in his westward course towards
Western Australia. In 1873 it was crossed by Mr. Gosse at a narrow neck near
its eastern extremity ; but in the next year Mr. Giles was again forced to retrace
his steps, the bed of the lake, where examined by him, being found to be so bogg
as to be impassable. In 1889 Mr. Tietkens examined the western portion of the
lake, and was consequently able to define approximately its true outline, which
had previously been extremely hypothetical. His examination of the lake
resulted in the shortening of its length, as shown on the maps up to that time,

by more than 100 miles.

Its extreme western portion, which was previously supposed to be situated
about 128° 10’ in Western Australia, and to be about twenty to thirty miles wide,
is now known to be situated in South Australia, about 130° 18’, and to be only

from two to three miles wide.

According to Mr, Tietkens, its extreme length is about ninety-two miles,
while its width varies trom two to fifteen miles, the maximum width of fifteen
miles occurring about the 131st meridian. At the narrow neck, however, where
we crossed, it is not more than three-quarters of a mile wide.

The area of the lake is approximately 700 square miles, and its altitude above

sea level must be more than 1000 feet.

One set of calculations of its elevation were based on Mr. Winnecke’s figures
for the altitudes of the camps at Bagot Creek and Reedy Hole, and on the
differences between the barometrical readings at those places and at Lake
Amadeus ; while another set were based on the barometrical readings given by

Mr. Tietkens in his Journal, etc.

As far as known, Lake Amadeus receives the drainage of a few small creeks
only, as no rivers of any importance have up to the present time been discovered
within the area of its basin. The view of the lake gained from the neighbouring
sandhills is a very remarkable one. Stretching away to the east and west as far
as the eye could discern was a dazzling, white, flat expanse, on whose surface no
water could be seen, but in its place a coating of a white saline material, which on
analysis proved to be composed almost entirely of common salt, with a small
amount of sulphate of lime (gypsum). On closer examination the saline crust was
found not to exceed a quarter to half an inch in thickness, under which was a red
argillaceous sand passing down into similar material of a grey colour. The surface

of the lake was found to be tolerably firm, the horses only sinking to the depth of

22 HORN EXPEDITION—PHYSICAL GEOGRAPHY.

a few inches. On each side of the lake the sandhills rise to a height of fifty feet,

and have a nearly east and west trend.

E.—CLAYPANS.

After the description of the lakes it is necessary to say a few words about
those miniature lacustrine features known as “claypans.” They are usually in the
form of flat shallow depressions, often nearly circular, but in the majority of cases
of irregular outline, and usually devoid of vegetation. They are generally
surrounded by loamy plains or sandhills, and while they are more frequently met
with throughout the Cretaceous area, they are still not uncommonly found on the
plains and in the valleys of the ranges within the Ordovician area. Mr. Streich
suggests that claypans owe their existence* to an ascent of subterranean water at
the junction between the “sedimentary and the metamorphic formations,” as he
found them numerous in the neighbourhood of the junction line. We, however,

observed no such relation, and give below our explanation of their formation.

Claypans vary in diameter from a few feet up to as much as three-quarters of
a mile, a common size being from fifty to one hundred yards. They are exceedingly
shallow, the depth of the bottom below the general level of the surrounding sand-
hills or plains is seldom greater than five feet, and usually much less, being in the
majority of cases not more than two to three feet. In some cases the edge of the
depression is ill-defined, the plain merging almost imperceptibly into the claypan,
and the only indication of the circumferential limits is the ring marking the edge
of the deposit of fine silt which covers the bottom and sides of the claypan. In
other cases the sandhills come to the very edge, and form a well-defined rim to it.
The area drained by them is limited to a very narrow peripheral belt. As a
general rule water does not remain in them very long ; some of the best hold water
for three or four months, but in the great majority of cases, especially of the smaller
ones, the water disappears from them at the end of a month or two. There are
exceptional instances, however, of which Conlon Lagoon is an example, in which

water would remain for very much longer periods.

The water of the claypans has generally a reddish-yellow colour, due to the
presence of a quantity of very fine mud of that colour held in suspension, which
on evaporation of the water is deposited on the bottom of the claypan as a fine silt
with a peculiar glazed surface, due perhaps to the extreme fineness of the last

portion of the sediment deposited. On drying, this mud loses water and splits in

* Trans, Roy. Soc. of South Australia, vol. xvi., part ii., p. 90.

HORN EXPEDITION—PHYSICAL GEOGRAPITY. 23

all directions, cracks as much as a quarter to half an inch wide making their

appearance and separating the more or less rectangular masses from each other.

The following explanation of the method of their formation has suggested
itself to us. They naturally occur only where the country is flat, “e., where the
slope of the ground is not decided enough in any particular direction to cause the
surface water to flow in that direction. There is therefore a tendency for the
water to lie on the surface, or rather to be gathered into slight depressions, which
are sure to exist even on otherwise almost level surfaces. At first the water that
was gathered into these slight depressions would almost immediately percolate the
porous strata, but in doing so it would leave behind a deposit of silt. This would
happen with every subsequent heavy fall of rain, until the silt suspended in the
water and carried into the depression and deposited there was in sufficient quantity

to prevent further percolation.

The claypan has now become established and will retain water for a longer or
shorter period, and as there is now very little percolation through the bottom there
will be no further settling of the floor as there may have been in the early stages.
The depth of the claypan in many cases will, however, be increased by the growth
of the rim by the deposition at the water’s edge of the fine particles of sand, ete.,
driven along the surface of the ground by the wind. In this manner the rim may
be added to from time to time, and the holding capacity of the claypan thereby

increased.

The largest example of a claypan seen during the Expedition is one that
occurs a few miles to the south of Heavitree Gap, and known locally as Conlon
Lagoon. In its greatest dimensions it is a quarter of a mile wide and_ three-
quarters of a mile long. The depth of the bottom of the lagoon below the
surrounding country does not exceed four or five feet, and as there was at the time
it was visited not more than three feet of water in it, it was already in process of
drying up. Where dry the bottom was seen to be formed of a clayey sand.
Conlon Lagoon lies between two ranges trending east and west, the drainage
from which finds its way into the lagoon. There is, however, no indication of an
outflow eastwards to the Todd (the only possible direction), the lagoon and the
ranges on the north and south forming a miniature internal drainage system of

their own.

F.—STONY PLAINS.

The whole of the area from the northern extremity of Flinders Range north-

wards to within a few miles of Mount Burrell Cattle Station on the Hugh River,

24 HORN EXPEDITION—PHYSICAL GEOGRAPHY.

and for many miles in an easterly and westerly direction, may be said to be
occupied by rocks of Cretaceous age, covered over large areas by Post-Tertiary
deposits and over very limited areas by Pliocene beds of lacustrine origin. The
upper strata of the Cretaceous system have been removed by denudation over
extensive areas, the remaining portions being in the form of more or less isolated
table-topped hills dotted about throughout the whole area. The materials set
free by this denudation have gone to form the superficial accumulations known

as “gibber” or “stony plains,” loamy plains, and to a large extent also the

sandhills.

“Stony plains” is the name given to those portions of the Cretaceous area
over whose surface are strewn “ gibbers,” ze, rounded or subangular fragments of
silicified sandstone or grit known as ‘desert sandstone.” The desert sandstone is
extremely hard and weather-resisting, and has a somewhat sub-conchoidal fracture.
With such properties it is not surprising to find fragments of it covering much
of the country from which the sandstone has been denuded.

The uniform distribution of the gibbers, which is a very characteristic feature
of this class of country, is due to the fact that the fragments derived from the
layer of “desert sandstone” which extended over this area, now strewn with
gibbers, have not undergone redistribution to any large degree. In a flat district
like this the surface water has not been able to sweep them into water-courses.
The removal of the argillaceous sand by the wind and rain has permitted the
gibbers to settle down, until in many places they present a flat surface resembling
an artificial pavement. The outer surface of the gibbers is of a dull red colour,
due to the presence of a thin film of oxide of iron coating them. They also present
a glazed sub-angular or pseudo-waterworn appearance, produced by the polishing
action of the sand grains as they are driven along the surface of the ground by

the wind.

The stony plains gradually merge into loamy plains, which possibly occupy the
sites of areas of the Upper Cretaceous, which were devoid of the ‘desert sand-

stone” capping.

On either sides of the banks of many of the rivers, especially along their
serpentine courses over the plains, are extensive alluvial plains. During floods
the channels are too flat and shallow to carry off the immense body of water that
occasionally comes down them, and the water spreads out on either side, sometimes
for miles. The “box flats,” which are met with on the sides of the Finke Channel,

are flood plains, on which Lucalyptus microtheca flourishes in large numbers,

HORN EXPEDITION—PHYSICAL GEOGRAPHY. 25

G.—SANDHILLS.

The last features of importance are the sandhills, which oecupy the surface
over immense areas of the interior. These are ridges of usually a red argillaceous
sand, having in many localities an approximately parallel arrangement, and there-
fore with a constant trend usually N.E and 8.W., due to the prevalence of S.E.
winds, but elsewhere occurring quite irregularly. The trend of the sandhills is to
a great degree dependent upon the direction of the prevailing wind, being almost
at right angles to this. Separating the ridges are the corresponding diminutive
valleys, the floor of which is usually of a much more clayey character than the
material of the sandhills. They have one steep fall inclined at an angle of about
30° and situated on the side opposite to the quarter from which the wind blows,

the other side having a gentler slope.

The sandhills rise to very varying heights, thirty or forty feet being a very
common height, while in some cases they reach seventy feet, or even in some
extreme cases 100 feet above the level of intervening flats. The highest sandhills
were crossed during the trip from George Gill Range to Ayers Rock, where also
the greatest development of them was seen. The surface of almost the whole of this
strip of country is occupied by sandhills, which are clothed over very large areas

with “porcupine grass” (Z7?todia).

CENA GEOROG

By PROMESSOK RALPH TATE and J. AN WATT «B.Sc

(With Puates 1 AND 2).

The geological features of that portion of Central Australia examined by us,
embracing the country lying between Oodnadatta on the south and the ranges
on the north, will be described under a number of headings. Under each of
these, bearing the names of the geological systems to which the different series
of rocks are assigned, a summary of the conclusions of previous observers and an
account of the general geological features, the extent, thickness, mineralogical
composition, petrological characters, and fossiliferous contents of the rock will be
given. Detailed descriptions of the fossils and of the microscopical characters of

the more important rocks form the subjects of separate papers.

I.—Previous Records and References to the ‘Literature of
the Region.

I.—Warernovse, F. G., “Features of Country on Stuart’s Track across
Australia,” Parl. Paper, 8. Aust., No. 125, 1863. The author was naturalist to
Stuart’s Transcontinental Expedition, and in his report makes incidental refe-

rences to geological features. He divides the country into : —

(1) The spring and salt-bush country extending from the Goolong Springs to
a little north of Hanson’s Gap (lat. 27°, 18’, 23”). The springs are stated to be of
volcanic origin (pp. 1, 3, 4), and as proceeding from volcanic lava and extinct
cones. Reference is made to the discovery of the remains of Diprotodon australis
at Hergott Springs (p. 2), and of fossil shells in an argillaceous rock, attributed to
the Tertiary age, at the Gregory and Welcome Springs (p. 2). [This formation is
now known to belong to the Rolling Downs system, and the mussel-shells alluded
to are Modiola inflata, Moore. |

(2) This division extends to the southern side of Newcastle Water (lat. 17°,
36’, 29”), and is described as somewhat sandy and occasionally stony and loamy
soil, with some considerable range of hills (p. 5). A geological section on the

banks of Finke River at Polly Springs, near Engoordina, is described in the

HORN EXPEDITION—GENERAL GEOLOGY. 27

following terms :—-“ At the bottom an argillaceous schist, above many horizontal
strata of a soft argillaceous rock, occasionally interstratitied with a free sandstone
of various hues ; at the top was a stratum, not very thick, of a peculiar siliceous
rock of a drab colour; it breaks with a conchoidal fracture and looks like very

hard baked earthenware ” (p. 5).

[The basal formation indicates an inlier of Pre-Cambrian age; the intermediate
argillaceous series represents the type of the Upper Cretaceous which prevails on
the northern confines of the basin ; the uppermost formation is of the usual, desert
sandstone, type.] The James and Waterhouse Ranges are constituted of a dark,
hard ferruginous sandstone (p. 5). [The characteristic rock of the Larapintine
Series (Ordovician) |. In the gorge of the Hugh River in McDonnell Range “ the
rock is a variety of gneiss of a very laminated nature.” [This description is more

apt than that of Stuart].

I].—Sruarr, Joun Macpoucari, “Journal of Explorations in 1858-63,”
London, 1864. The first geographical exploration of the region under review was
by Stuart on three separate occasions embraced in the years 1858-1862. He
describes the axis of the McDonnell Range, particularly at Brinkley Bluff, as

consisting of granite.

III.—Gossr, W. C., “Exploration in 1873,” Parl. Paper, 8. Aust., No. 48,
1874. [The determinations of some of the rocks referred to by Gosse are based
upon the examination of the original specimens in the Museum of the School of
Mines at Adelaide]. The author describes the rock-structure of Mount Liebhig,
the most westerly point of the McDonnell Range, as composed of basalt, gneiss,
and sandstone ; strike E., dip 14° 8.; the rock (-face) perpendicular for £00 and
500 feet on south side. [The original specimens are gneiss, hornblende-schist, and
quartzite}. A granite ridge between Mounts Liebig and Udor has a strike
E.x8., dip 4° 8. [A rock labelled Mount Udor is an example of Ordovician
quartzite]. The ridge of the West Bluff Hills is composed of gneiss ; strike S.E.
x E., dip 81° 8. Mount Palmer is composed of granite, gneiss, sandstone and
puddingstone ; strike W., dip 15° north. [Rock specimens labelled King’s Creek,
George Gill’s Range, are limonite and a fine-grained compact sandstone of
Ordovician age}. “ Ayers Rock is a high mass of granite 1100 feet above the
surrounding country.” [A specimen labelled Ayers Rock is a small rolled

fragment of epidote-hornblende. |

TV.—Gixes, Ernest, “Geographic Travels in Central Australia from 1872-
; ) gray

1874,” Melbourne, 1875. The chief geological records by this explorer, which
b b] fo) Oo 4
A

28 HORN EXPEDITION—GENERAL GEOLOGY.

the authors have had the opportunity of personal investigation, are :—‘‘ Chambers’
Pillar is composed of a loose white sandstone” (p. 6). ‘‘Johnston’s Ranges had
the very red appearance of red sandstone, and had a series of ancient water-marks
along their sides” (p. 7). ‘The ranges by the Finke River, two miles north of
McMinn’s Creek, are composed of red sandstone, stony and precipitous, 800 feet
above the plain” (p. 11). ‘ McDonnell Range is formed of three separate lines of
hills, running east and west, the most northern the highest, fully 4000 feet above
sea level ; the other two lines may be called only foot-hills, the most southern and
lowest is formed of sandstone, the middle tier is basalt, and I believe the main
chain is of basalt also; the southern flank I found to be composed of pudding-
stone” (p. 17). ‘Gosse Range is composed entirely of red and white sandstone ”
(p. 19). “The higher mountain beyond (Mount Tate of Winnecke) was girt
around by a solid wall of basalt, fifty or sixty feet in height, from the top of which
the summit rose” (p. 22). Sandstones occur at Glen Edith (p. 43); the George
Gill’s Range is composed of enormous masses of red sandstone (p. 58). Mount
Olga is formed of several vast and solid rounded blocks of bare red-coloured stone

of a kind of conglomerate (p. 95).

V.—Smytu, R. Broveu, “First Sketch of a Geological Map of Australia,”
Melbourne, 1875. The James and Gardiner Ranges and the McDonnell Range
west of the Finke River are coloured as granite within an area of metamorphic
rock, which extends west to Alice Springs. Metamorphic rock in a small area is
shown resting on the west bank of the Finke River, extending from Charlotte
Water to the Lilla Creek. The rest of the Larapintine and southward to the
Macumba River is represented as Tertiary.

VI.—Cuewines, C., published in 1886 a sketch-plan of the Larapintine area
as the outcome of personal survey, on which is represented, by shading, basalt,
sandstone, and granite :—‘‘The McDonnell Ranges are composed chiefly of
basalt ; though sandstone and granite are plentiful, the basalt formation forms
the backbone, frequently rising 2000 odd feet above the plain.” [Basalt is
indicated as forming the higher levels of the escarpment of the George Gill, Levi,
and Middle Ranges and elsewhere, the rest of the rocky country being represented

as composed of sandstone. |

VII.—Department or Minus, Vicroria, “Geological Map of Australia,”
Melbourne, 1887.—The metamorphic area on the west bank of the Finke River,
between Charlotte Waters and Lilla Creek, of the former map is herein repre-

sented as Lower Paleozoic ; the east side is coloured as Cretaceous, and the area is

HORN EXPEDITION—GENERAL GEOLOGY. 29

extended northward to include Chandler’s Range. The Levi and George Gill
Ranges are indicated as Tertiary, whilst the main portion of the Larapintine is
represented as granite and Newer Volcanic, except a small patch around Alice

Springs which is coloured as metamorphic.

Up to this date the work done has little claim to serious attention, as. it
consists almost solely of locality-records of a few kinds of rock-masses ; no attempt
had yet been made to indicate their stratigraphical relationships, except in the
sole instance by Waterhouse, respecting the section at Polly Springs. Some
excuse may therefore be found for the imperfection of the two geological maps
issued by the Victorian Government, the compilers of which had no other data
before them than such bare records as we have sketched herein. The information
had to be taken for what it was worth or wholly rejected ; hence the great blot of
volcanic colouring on the later map, which error is traceable to Giles, and was
repeated and enlarged upon by Chewings. Their basalts are the thick quartzite

bands in the Larapintine Series, and perhaps also those of the Pre-Cambrian.

Vil.—Kast, J. J., “On the Geological Structure and Physical Features of
Central Australia,” Trans. Roy. Soc. 8. Aust., vol. xiL, pp. 31-53, pL iii, 1889
(Read 2nd April).—Being observations made along the Overland Telegraph Line
from Lake Eyre to the McDonnell Range, and deals with the south and north-east

parts of the country traversed by us.

Topographical Features.—(1) “The Great Austral Plain” embraces the low
level country about Lake Eyre and the table-topped hills and small tablelands
which arise from it—a vast region of inconsiderable elevation. Sterile patches
covered with glazed subangular stones are herein called ‘“ gibbers.” (2) ‘The
Terraces ” embrace the parallel ranges of low altitude, separated by broad valleys
or plains, commencing near the junction of the Hugh and Finke Rivers. [The
term “terraces” is inapt], (3) “The Great Central Plateau,” the southern
boundary of which is the McDonnell Range, whose furrowed southern face
developes the system of narrow ridges collectively known as the MeDonnell
Ranges. [This description, as also the section, pl. iii., fig. 6, is misleading, as the
general altitude of Burt Plain, to the north, is the same as that of the river-

valleys in the McDonnell Range].

Geological Structure.—(1) Outliers of the Flinders Range from Finnis Springs
to Mount Dutton are classed as Archean |Our observations incline to the
opinion that, though the Peake Range is doubtlessly Pre-Cambrian, yet the fissile

limestone and associated strata from tho Neales River to Mount Dutton belongs

30 HORN EXPEDI'TION—GENERAL GEOLOGY.

to the Cambrian]. (2) The beds of the table-land of the Great Austral Plain in
the vicinity of Dalhousie Springs are described as consisting of a great argillaceous
series crowned by porcelainised sandstone ; they are considered ‘to be Mesozoic
(and probably Cretaceous).” The porcelainisation of some of these strata is
considered to be due to submergence in silicated waters which are wholly
evaporated (p. 51); and it is noted that “the obsidian bombs are most numerous
among the portions of the plain whose surface is strewn with chalcedony and
ironstone nodules” (p. 53). The foundation rocks of “the Terraces” consist of
fissile sandstones, argillaceous and siliceous limestones, as in Mount Charlotte
ridge, and appear in gentle undulations, which become more and more sharply
curved on approaching the McDonnell Range (pp. 46, 51). The central plateau
consists of impure limestone and an underlying red quartzite, which forms the
south edge of the central plateau and rests on gneiss and granite intersected by
diorites—the whole, from Lake Eyre to the Burt Plain, representing a conformable
series (p. 47), though a doubt is expressed with regard to the rocks of the
McDonnell Range, which, on the ground of their degree of metamorphism, may
perhaps be considered Archean (p. 51). [(3) Nevertheless, the schistose rocks at
Polly Springs are compared with the primary rocks of Denison Range]. (4) De-
scribes gravels containing large boulders of granite and schist on the north flank
of Cunningham Gap, and suggests their derivation from “a bar of primary rocks,”

of which those at Polly Springs may be a remnant (p. 44).

1X.—Brown, Henry Y. L., “ Report on a Journey from Adelaide to Hale
River,” Parl. Paper, S.A., No. 24, 1889, with Map and Sketch Section. “From
Mount Dutton northward to the vicinity of Mount Burrell the whole country is
occupied by the Cretaceous and Tertiary formation.” Extinct mound-springs are
stated to occur at Dalhousie Head Station. In the vicinity of Mount Burrell,
commencing three miles south from it, are crystalline limestones with flinty veins,
quartzite slaty sandstone and cleaved slates; these are considered Primary (pro-
bably Silurian). Overlying these, first seen at and northward of Ooraminna Well,
are brown and white sandstones, which are classed by the author as Devonian (!) or
Silurian. The red quartzites and overlying beds which form the southern barrier
of the McDonnell Ranges are included with the granitic and metamorphic rocks

which compose the main ranges under the head of Azoic.

X.—Brown, Henry Y. L., “Report of Geological Examination of Country
in Neighbourhood of Alice Springs,” Parl. Paper, 8.A., No. 189, 1890. The
fundamental rocks of the McDonnell Ranges are various metamorphic rocks with

eruptive dykes of diorite, pegmatite and coarse granite. Resting unconformably

HORN EXPEDITION—GENERAL GEOLOGY. 31

upon these are quartzites (sometimes conglomeratic), dolomitic limestone, and
occcasionally clay-slates, and are classed as “Cambrian (%).” In the main valleys
of the ranges are flat-topped hills of quartzite, conglomerate, ironstone, and ferru-

ginous sandstone ; these beds belong to the Secondary or Tertiary age,

XI.—Cuewines, Caries, “Geological Notes on the Upper Finke Basin,”
Trans. Roy. Soc. 8.A., vol. xiv., pp. 247-255, pl. x., 1891. The stratigraphical

sequence as established by the author is as follows :—

Pre-Strurtan.—Developed in the McDonnell Ranges. [Certain limestones

and shales are included, which the writers refer to the next series. |

Siturian. —Comprising the “ McDonnell Ranges south.” This assigned posi-
tion is based on the fossil evidence as interpreted by Prof. Tate (p. 255). [ Herein

are included the Post-Ordovician conglomerates of the present writers. |

Drvontan.—Rocks of this age occupy, according to the author, the synclinal
folds of the Silurian quartzites ; to which also belongs the Ooraminna sandstone.

| These we fail to separate stratigraphically and structurally from the Ordovician. |

Mesozorc (?)—To this period belong a coarse sandstone formation, forming
flat-topped hills in the heart of the McDonnell Range. — [The development at Glen
Helen Station referred to by the author consists of the residue of the waste of the
eneissic and granitic rocks, and offers no analogy to the Cretaceous rocks on the

southern borders of the Primary as suggested by Brown (x., p. 2).|

Crrraceous.—A limestone rubble with flints and gypsum resting uncon-
formably on the supposed earlier Mesozoic rocks, at the junction of the Palmer

and Walker Creeks, is in the opinion of the writers a recent travertine.

Tertiary.— The cone-shaped hills composed of clay-grit, horizontally bedded,”
as seen by us at the extreme of Petermann Creek, on the Walker, and Vale of

Tempe, are outliers of low-dipping Ordovician sandstones,

XII.—Brown, Henry Y. L., “Report on Leigh Creek Coalfield,” Parl. Paper,
No. 158, 1891, p. 12, states that “lying unconformably on the crystalline meta-
morphic, gneissis, and granitic archaean rocks of the McDonnell Ranges there are
two other rock-systems unconformable to each other. The lower of these consists
of quartzite, quartzite conglomerate, dolomitic limestones, ete., striking EK. and W.
. . . indescending the Finke they appear at intervals as highly-inclined beds,
the outcropping edges of synclinal troughs in which rest the upper system. — [These

are referred to Cambrian.| The upper system consists of sandstone quartzite,

32 HORN EXPEDITION—GENERAL GEOLOGY.

shale, and thin bands of limestone, also striking EK. and W. . . The George
Gill and James Ranges are composed of these rocks. It is from these that Silurian

fossils were obtained.”

XI1I.—Tierkens, W. H., “Journal of the Central Australian Exploring
Expedition,” Adelaide, 1892. In 1891 Mr. Tietkens, in command of a prospecting
party, started from Alice Springs, skirting the north front of the McDonnell
Range to Mount Heuglin, thence to Mount Sonder and Glen Edith, and west-
ward beyond the West Australian boundary; on his return route he examined
Mount Olga and Ayers Rock. A catalogue of the rock-specimens collected by
Tietkens is furnished by Mr. H. Y. L. Brown (Appendix, pp. 82-84), who also, by
sketch-sections, shows the stratigraphical structure of the McDonnell Range west
of Mount Sonder, and of Mount Olga and Ayers Rock., Mount Sonder to
Mereenie Bluff, Mount Olga and Ayers Rock are coloured to represent ‘ Meta-
morphic metal-bearing rocks” overlying granite. The quartose sandstone at Glen

Edith is referred to “ Paleozoic (Devonian ?).”

XITV.—Brown, Henry Y. L., “ Further Geological Examination of Leich’s
’ b) fon) t=}

Creek and Hergott Districts,” Parl. Paper, S.A., No. 23, 1892. The Government
Geologist made “a brief and rapid examination of the Finke River region in

g Pp s
September, 1890,” and herein, under the title of “General Geology on the Finke
River,” p. 7, he amends his previous outline description which is illustrated b

+} p ’ Pp Wy
an ideal section from the McDonnell Range to Charlotte Waters.

The fundamental rocks are classed as ARCHMAN; the quartzites, dolomites,
limestones, sandstone and slate which crop-out in anticlinal arches on which the
succeeding formation rests apparently unconformably are classed as CAMBRIAN.
The Post-Ordovician conglomerates at the Finke Gorge are here included. The
author records that the metamorphic granitic rocks dip under quartzite at Mount

Sonder and in a southerly direction are succeeded by highly inclined dolomites, ete.

Lower Siturtan. According to this author, the rocks of this age commence
in the range bounding the Missionary Plain on the south, and extend south to
Henbury and Ooraminna, the only distinction from the foregoing is “a less
disturbed rock-formation.”

XV.—Cuewines, CuHarues, “Notes on the Sedimentary Rocks in the
McDonnell and James Ranges,” Trans. Roy. Soc. 8.A., vol. xviii., pp. 197-199,
1894. This is, in part, a correction of previously published opinions (xi.) and a

criticism of Mr, Brown’s classification (xii, and xiv.); his grouping is as follows :—

GENERAL GEOLOGY. 33

HORN EXPEDITION

Founpation Rocks, previously called Pre-Silurian. Giren Heven Series (Cambrian
and Pre-Cambrian ?) is introduced by a quartzite, overlain by crystalline lime-
stones, dolomites, clay-slate, etc.; rising through the eroded Lower Silurian
anticlines. MaArreno Biurr Serres (Lower Silurian part) embraces the fossil-
iferous limestones and associated sandstone and quartzites. WALKER Creek Series
(Devonian?) ; as previously, the author regards these beds as unconformable
with the Ordivician, whereas we recognise them as only the more gently

undulating Larapintine sandstones (Ordovician).

II.—Pre-Cambrian.
(a) Introduction.

Much attention has of late years been paid by geologists in Great
Britain, on the Continent of Europe, and in North America to the study of
the important but very complex series of rocks variously known as Archiwan,
Azoic, Pre-Cambrian, ete., which underlie unconformably the base of the O/ene//us-
zone of the Cambrian system wherever it is developed. The result of this laborious
work has been the establishment of our knowledge of the origin, tectonic structures,
and geological relations of the different members of this heterogeneous division of
rocks, and their relation to the overlying Paleozoic fossiliferous strata on a sounder
basis. Unfortunately very little work of a similar nature has been done in
Australia, where the extensive and easily-accessible areas of Pre-Cambrian rocks
of Yorke’s Peninsula and the Mount Lofty Range offer special facilities for such a
study. Not many years ago the majority of the geologists were inclined to group
all rock-masses that had been subjected to regional metamorphism, and had taken
on characters of a certain nature in one class and include them all under one name,

such as that of Archean.

This system was supposed to include the original crust and all sedimentary
strata deposited by the water of the ocean before it had cooled down sutticiently
to permit life to appear in it. By others they were considered to represent
originally sedimentary rocks comparable to the later fossiliferous strata, which
had been subjected to enormous compression, undergoing thereby great physical
and chemical changes. In many cases the planes of foliation and cleavage were
interpreted as planes of stratification. These views have undergone considerable
modification. In the first place many areas of metamorphic rocks have been
relegated to their proper positions in the geological record as highly-altered
Palieozoic, Mesozoic, and even Tertiary sediments. It is furthermore believed that

the areas coloured on the geological maps as Paleozoic, Mesozoic, and Tertiary will

34 HORN EXPEDITION—GENERAL GEOLOGY.

still further increase at the expense of those coloured Pre-Cambrian in proportion
as these areas are subjected to more rigorous and searching examination. Accord-
ing to some of the highest authorities of the present day the Pre-Cambrian rocks
can often be divided into two great groups, one including the rocks of eruptive
origin, the other those of sedimentary origin. In the first division are included
the gneisses, schists, and eruptive rocks, which underlie uncomformably Cambrian
strata, or, where members of the second group are developed, either underlie them
unconformably or intrude them. In the latter case the gneisses are of later date
than the rocks of the second group. In the second group are included the rocks,
which can be proved to have had a sedimentary origin. These usually overlie the
gneisses, etc., of the first group. As an example of such a classification we may
take the two groups of rocks of Pre-Cambrian age, which are developed in North-
west Scotland, and known as the Lewisian gneiss and the Torridon sandstone.

The former underlies the latter, and the latter the Cambrian strata unconformably.

In North America the Pre-Cambrian rocks have been divided into two great
groups corresponding somewhat to those made out in Scotland. The lowest and
oldest, consisting of gneisses, mica, schists and granites, are included under the
name of ‘Fundamental Complex.” This great group is overlain unconformably
by an enormous thickness of more or less highly altered sedimentary rocks, and

intercalated volcanic lavas and tufts.

This latter American group, to which the name “ Algonkian” has been
applied, has been again divided into three groups, each separated from those above
and below by strong uncomformabilities. The total thickness of this latter division

has been estimated at 65,000 feet.

In the uppermost strata of the Algonkian group distinct traces of fossils have
been detected by Mr. Walcott.*

In Brittany too, Dr. Barrois has discovered organic remains in the form of
Radiolaria in rocks of Pre-Cambrian age, which there consist of graphitic quartzites.
At the meeting of the British Association for the Advancement of Science at
Oxford, August, 1894, the supposed organic nature of the bodies termed Radiolaria
by Dr. Barrois was called in question, the chief arguments against their organic
origin being based on their very minute size, their diameter being on the average

only about one-sixteenth that of the average diameter of recent Radiolaria.

The Pre-Cambrian area of Central Australia area is, geologically speaking,

practically a terra incognita. Our visit to this inaccessible region extended over

* Tenth Annual Report U.S, Geol. Sury., 1890, Walcott, p. 552,

HORN EXPEDITION—GENERAL GEOLOGY. 35

only a week or two, while the distance to be traversed during that time amounted
to many hundred miles. The geological visits of others have been equally brief,
and undertaken under similar unfavourable circumstances. Thus no detailed
study of the rocks was possible ; all that could be done was to gain a general idea

of the whole, and to make, as far as possible, a typical collection of the rocks.

The occurrence of granite or gneiss in the McDonnell Range was made known
first by Waterhouse (1) and Stuart (2), and subsequently recorded by other

travellers.

Mr. J. J. East (viii, p. 51) makes the following statement :—‘ It is a reason-
able presumption that the beds throughout” (this region, Ze., from Lake Eyre to
Everard Plain) “belong to one great series.” As Cretaceous fossils had been found
as far north as Mount Daniel, he concludes that the rocks of the whole region all
belong to that system. He thus includes in the Cretaceous system strata that we
now know to contain fossils of Ordovician (Lower Silurian) age, and a series of
rocks underlying these unconformably, and now termed Pre-Cambrian. Such an
hypothesis would have been at any time a most improbable one, and at the present
time its acceptance is of course out of the question. ‘ But should their age,”
continues Mr. Hast (referring to the rocks of the McDonnell Ranges), ‘be
considered Archean solely on the ground of their high degree of metamorphism?”
This author attributes the metamorphism of the rocks of the McDonnell Ranges to
the presence of ‘diorite” intrusions. This theory cannot commend itself to
anyone who has observed the enormous area occupied by these rocks, and their
high degree of metamorphism on the one hand, and the comparatively small size,

and in places almost entire absence, of such ‘“ diorite” intrusions on the other.

This region clearly furnishes an almost typical example of regional meta-
morphism, in which great changes, both physical and chemical, have been produced

in the rocks by extensive earth-movements.

Mr. H. Y. L. Brown (ix.) speaks of the “granite and metamorphic country,”
and describes the occurrence of garnets and beryl in these rocks. In the sketch-
section and map accompanying that report, these rocks are called “ Primary

Rocks (Azoic).”

The same author (x., p. 1) describes the rocks of the McDonnell Ranges as
“Metamorphic and Plutonic Primary Rocks;’ and mentions as occurring there
“miieaceous and hornblendic gneiss, micaceous, hornblendic siliceous, and argillace-
ous schists and slates; syenite, garnetiferous granite, micaceous granite; epidocite ;

dolomite and crystalline limestone, with eruptive dykes of diorite, pegmatite and
OA

36 HORN EXPEDITION—GENERAL GEOLOGY.

coarse granite.” He also points out that they show “signs of stratification ” and
“dip at varying angles.” The presence of quartz reefs is also mentioned by the
same author, and in a later portion of the same report a detailed description of the
principal alluvial diggings, and auriferous reefs in the vicinity of Artunga is

given.

Mr. Chas. Chewings (xi., p. 247) calls the series of rocks under consideration
Pre-Silurian. This he did on the evidence of their unconformability and inferior
stratigraphical position to rocks containing fossils ascribed by Prof. Tate to the
Upper Silurian. This was, of course, under the circumstances, a safe provisional
conclusion. There are, however, many weighty reasons why, in the light of our
more extended knowledge of them, they should now be more definitely termed
Pre-Cambrian. He asserts also that they are “ distinctly stratified, with a dip in
general to the north at a steep angle.” He next gives what he considers to be
the order of succession of the rocks, commencing from the north side of the
‘McDonnell Ranges, as follows :—Chlorite-schist, granite, ‘‘micaceous schists and
metamorphic granite, with occasional outcrops of coarse eruptive granite and
other eruptive rocks,” quartzite, ‘‘metamophosed clays and _ shales, interstratified

with yellow and blue crystalline limestone.”

Mr. H. Y. L. Brown (xii., p. 12) points out that, overlying unconformably ‘the
crystalline, metamorphic, gneissic, and granitic Archzan rocks of the McDonnell
Ranges, there are two other rock systems, unconformable to each other,” which he
calls respectively Cambrian and Lower Silurian. Ina later report (xiv.) he calls
these metamorphic rocks Archzan, a name which for many reasons it would be

better to replace by Pre-Cambrian.

Prof. Tate, in referring to the Pre-Cambrian rocks of Australia in his
Inaugural Address to the Australasian Association for the Advancement of Science
in 1893,* thinks “that there are good reasons for the belief that these rocks, which

?

exhibit the phenomenon of regional metamorphism, belong to one epoch ;” and he

goes on to say that “the chief evidence” (for the above statement) ‘is that they

occupy parallel lines of elevation, having an approximate north and south bearing.”

A uniform meridional trend, however, in the axis of folding of regionaily
metamorphosed rocks does not appear to be a safe guide as to the Pre-Cambrian
age of all such Australian rocks as exhibit it, as the trend of the lines of elevation
and foliation oceupied by the metamorphic rocks of the McDonnell Ranges are
nearly due east and west, and it is now known that these rocks are Pre-Cambrian.

* Rep. Austr. Assoc. Ady. Sci., Adelaide, 1893, p. 45.

e

HORN EXPEDITION—-GENERAL GEOLOGY. on

(6) Age.

In view of the present limited state of our knowledge of these rocks it is
evident that it is not advisable to employ such terms as Archean, Azoic, ete.
The first implies a greater knowledge of the relation of these rocks to those called
Archean elsewhere than we are in possession of, while the second has been shown
to be inadmissable by the discovery of fossils in Pre-Cambrian rocks in North
America and France. The best term, if a local name be not desirable, and that
strongly recommended by Sir A. Geikie, is Pre-Cambrian. It may, however, in
the present case be objected that we have no reliable evidence that these highly-
altered rocks in Central Australia are older than the Cambrian, in which case a
still more general term such as Pre-Silurian would be necessary. We base our
belief that there is, nevertheless, every reason to consider their age to be Pre-

Cambrian on the following considerations :—

1. In the first place the fact that a very strong unconformity separates them
from the Lower Silurian group of rocks inakes it evident that they must be either

Cambrian or Pre-Cambrian.

9. We favour the latter alternative because :

(a) The enormous differences in the lithological characters and tectonic
structures of these two groups of rocks implies a vast lapse of time

between their respective dates of formation.

(8) In the above-mentioned features they differ from the known Cambrian
strata of Yorke’s Peninsula, and from those of Flinders Range in

South Australia.

(y) Their apparent lithological and structural similarity to the Pre-Cambrian
rocks of South Australia, as developed in the Mount Lofty Range.

(6) No eruptive dykes have been noted in Central Australia amongst the
Lower Silurian rocks, whereas they are very numerous amongst the
Pre-Cambrian, and exhibit different stages of metamorphism in the
same district, which tends to show that they have been intruded at
different periods. Some were probably intruded during the Cambrian
era. The process of metamorphism was undoubtedly a very slow
one, extending over a lengthy period. As it progressed intrusive
dykes made their appearance from time to time, the latest being, of
course, cvterts partbus, least altered. If then the highly metamor-

phosed rocks of Central Australia were of Cambrian age, surely

38 HORN EXPEDITION—GENERAL GEOLOGY.

some of the eruptive dykes, at least those that appeared last, would
have penetrated the Ordovician strata.

(c) There is an entire absence of fossils in the metamorphic group, whereas
even the Lower Cambrian rocks of Yorke’s Peninsula and the
Flinders Range in South Australia, and of the Kimberley district

in West Australia, have been proved to be fossiliferous.

The evidence obtained by us points to much of the metamorphic group having
had an eruptive origin, whereas the Cambrian rocks of Australia, as far as at
present known, are entirely sedimentary. No definite correlation will be attempted
between this group of rocks and others of apparently the same nature elsewhere in
Australia, inasmuch as no test of contemporaneity or homotaxial origin has yet
been discovered for rocks of Pre-Cambrian age. Similarity of mineralogical
composition cannot be depended on as a basis of correlation even among Cambrian

and Post-Cambrian strata, and much less in the Pre-Cambrian.

Paleontological evidence obviously entirely fails us. Lastly, the test of its
stratigraphical relations, even had Cambrian strata been proved to overlie the
metamorphic group unconformably, would have been inadmissible, in view of the
possible divisibility of the Australian Pre-Cambrian group, like that of North
America, into a number of sub-groups, separated from each other by strong uncon-

formabilities.

A few words, however, on the Pre-Cambrian rocks of other parts of South
Australia may be of interest in this place. The best known and most important
developments of undoubted Pre-Cambrian rocks are to be found in Yorke’s Pen-
insula and in the Mount Lofty Range and its N.N.E. extension. In the Mount
Lofty Range, according to Prof. Tate,* the Pre-Cambrian rocks occupy a vast

monocline, dip to the 8.E., and are not less than ten miles in thickness.

The peculiar feature of these rocks is the greater degree of metamorphism
exhibited as we ascend in order. At the base clay-slates, quartzites, and lime-
stones occur, undoubtedly sedimentary rocks altered to a greater or less degree.
These pass upwards into mica-schist, gneiss, and even granite, rocks partly at least
of a probable eruptive origin. No explanation of this apparent anomaly has been
given.

At Black Point, near Ardrossan, on the east coast of Yorke’s Peninsula, true

Pre-Cambrian rocks occur underlying uncomformably limestones of Lower Cam-

brian age, containing a trilobite and coral fauna characteristic of that age.

* Op. cit., p. 47.

HORN FXPEDITION—GENERAL GEOLOGY. 39

Some of the fossils described by Mr. R. Etheridge, jun., in his paper “On
some Australian species of the Family Archeocyathinwe ” came from Kanyka and
Blinman, in the Flinders Range, occurring in siliceous limestones. These fossili-
ferous limestones, according to Prof. Tate, “overlie unconformably the metamorphic
rocks which occupy the country to the eastward, bordering on the New South
Wales frontier.”

(c) Extent.

In journeying north from Oodnadatta a sudden and_ striking change is
observable in the lithological character of the rocks at the point where those
of Pre-Cambrian age succeed the Lower Silurian, four or five miles south of
Alice Springs Telegraph Station. Leaving quartzites and limestones we at once
find ourselves among rocks of a highly metamorphic character, such as gneisses

and schists of various kinds.

The lowest member of the Lower Silurian series is a hard, dense quartzite,
which rests inclined at a high angle unconformably on Pre-Cambrian gneiss. This
quartzite rises to an altitude of from 500 to 1000 feet above the plain, and forms
to a great extent the southern slope and the summit of a very prominent ridge.
On the northern slope of this ridge the quartzite forms a steep perpendicular face
for about 200 feet down from the summit. The remainder of the slope is formed

of the gneiss.

This prominent ridge, the northern face of which exhibits the junction line
between these two great systems of rocks, viz., Lower Silurian and Pre-Cambrian,
is traceable almost continuously in a nearly east and west direction for many
miles, at least as far as Mount Benstead on the east and Belt Range on the west.
In a northern direction the Pre-Cambrian rocks extend to the Burt Plain, forming
rugged mountains with intervening broken country of a rough hilly nature. ‘Their
further northern extension is concealed by a superficial covering of sand and

alluvium of weolian and fluviatile origin.

This plateau, known as the Burt Plain, with its covering of comparatively
recent deposits, rises to an elevation of over 2000 feet above sea level. Out of
this plateau there rise the Strangways, Reynolds, and Hart Ranges, all probably

composed of these ancient rocks.

The Hart Range, where examined, viz., near Mount Brassey, and again
twenty to thirty miles west of that point, was found to be entirely composed of

these rocks, Their eastern and western boundaries are not known. Southerly

40 HORN EXPEDITION—GENERAL GEOLOGY.

they disappear under the quartzites and limestones of Lower Silurian age, appear-
ing at the surface, according to Mr. Kast, as a low ridge, which crosses the bed of
the Finke eighteen miles above Crown Point Cattle Station. Still further south
they probably form a great part of the Peake and Dennison Ranges; and lastly,
a great part of the country to the east of Flinders Range is composed of them—
at all events of Pre-Cambrian rocks—being in several localities found to be over-
lain by strata containing Cambrian fossils. In the McDonnell Ranges alone they

occupy an area of at least 10,000 square miles.
(2) Structural Features.

Messrs. Brown and Chewings both state that the Pre-Cambrian rocks are
distinctly stratified, and have a definite and determinable dip. No evidence is
given in support of these statements, which must therefore be received with
caution. In the first place they appear to be conclusions from the unwarrantable
assumptions that the rocks of this region are metamorphosed sedimentary strata,
and that the planes, which are so strongly marked in many localities, are those

of bedding.

The evidence in favour of the eruptive origin of large areas of the Pre-
Cambrian rocks will be gone into more fully later. In the meantime we may
point to the porphyritic gneissic granite on which Alice Springs Telegraph Station
is situated, and which covers a large area, and to the augen-gneiss with lenticular
“eyes” of comparatively unaltered granite embedded in a ground mass of crushed
granitic minerals, as being strong evidence of the eruptive origin of rocks covering

large areas.

Although it may be possible and even in places probable that the planes,
which are so strongly developed, coincide with the original planes of stratification
in any large area where sedimentary rocks may have been developed, yet as a
general rule there can be no doubt that these planes represent foliation planes.
This statement is greatly strengthened by the facts of the coincidence over large
areas of the strike of these planes, and of their great persistency ; for they are
traceable not only through rock-masses, the eruptive origin of which it highly
probable, but also even through undoubted intrusive dykes. They are, therefore,
planes of foliation, of stratification-foliation—that is, of foliation corresponding
with the original bedding planes, it may be in places; but elsewhere assuredly

they appear to be those of cleavage-foliation.

The foliation and extreme degree of schistocity, and the development of planes

of shearing and cleavage resulting from the yielding of the rocks to the lateral

HORN EXPEDITION

GENERAL GEOLOGY. 4]

crust-pressure, give the rocks a bedded appearance. When, however, we trace
these pseudo-strata along the surface in the direction of their strike, we find that
many of them are not persistent even for short distances, but pinch out so as to
have the shape of lenticular masses. When therefore we speak of the direction of
strike and angles of dip of these Pre-Cambrian rocks, such terms must be considered
to apply to the planes of foliation. Rocks exhibiting all degrees of foliation
appear to be present from the coarse-banded gneissic granite from Alice Springs,
in which the foliation is scarcely noticeable in hand specimens, to such finely-
banded gneiss as that which is largely developed near the head of Ellery’s Creek.
In the Belt Range the dip of the foliation planes increases from 40° on the south
to 60° and 70° on the north side of the range. The foliation planes of the gneiss
near Slip-panel Gap, about sixty miles west of Alice Springs, strike N.E. and S.W.,
and dip at high angles to N.W. Further east, on the south side of Mount Conway,
the strike was found to have changed to E.N.E. and W.S.W., the dip being about
7O°S.S.E. Still further to the east, between the last-mentioned place and Alice
Springs, the strike was observed to be E.S.E. and W.N.W., while the dip had
decreased to 37° S.S.W. To the north and south of Alice Springs the foliation
planes of the gneiss dip at 40° to 50° S.W., the strike being N.W. and 8. E.

In the McDonnell Ranges, to the east of Alice Springs, the strike was the
same as that noted north and south of Alice Springs, but the dip had decreased to
25° S.W. On the banks of Jessie Creek, ten miles east of Alice Springs, the strike
of the gneiss forming the low hills there was N.E. and 8.W., and the dip about
40° N.W. In the Hart Range the planes of foliation were found to be well
marked; their strike varies from W.S.W. and E.N.E. to 8.W. and N.E., and the
dip observed varied from 50° to 60° in a direction varying from N.N.W. to N.W.
Lastly, in the Strangway Range, at Winnecke’s Depot, the gneiss was seen to dip
at 45° N. 10° KE. There is a remarkable absence of evidence of the original planes

of foliation having been subjected to any subsequent contortion, on either a lar

ee
or a small scale, a fact which seems to imply that the direction of the pressure was
constant for a prolonged time, and that the rock-masses were able to find relief
from the stresses to which they were subjected by the development of gliding

planes and sheer planes.

(e) Matertal Geology.

The rocks of this group may, for purposes of description, be roughly classified

as follows :—

1. Those whose sedimentary origin is evident.

42 HORN EXPEDITION—GENERAL GEOLOGY.

2. Those about whose origin there is considerable doubt, including a
great part of the gneisses.

3. Those that are clearly of eruptive origin. -

1. The only representatives of this division met with were the quartzites and
micaceous slates, whose exact stratigraphical position is rather doubtful. The
Pre-Cambrian at Gill’s Pass, on the Hugh River, is introduced by a thick mass
of quartzite, succeeded by micaceous schists and gneiss ; and in Stuart’s Pass, too,
quartzites are intercalated as we approach the axis of elevation in the gneissoid
granite of Brinkley’s Bluff. Representatives of this division were also found near
the head of Ellery’s Creek, forming an elevated ridge (vide Fig. 10) on each side, of
which undoubted Pre-Cambrian rocks occur in the form of gneisses and schists,
accompanied by intrusive rocks. This ridge is composed of highly-altered glassy
quartzites and micaceous clay slates, apparently passing into mica schist, quartzites,
and clay slates, which dip at 85° N., their strike being W. 10° N. We have not
enough evidence to determine whether or not these rocks belong to the Pre-
Cambrian. Their relation to the gneisses on the south and north sides of the
ridge was not made out. It is therefore quite possible that they may belong to
the Ordovician System, and form a portion of a northern extension of that system,
which had been faulted down so as to present the appearance of forming part of
the Pre-Cambrian System. On the other hand, it is also possible that they may
represent Pre-Cambrian sedimentary strata, which have been intruded by granites
of Pre-Cambrian age, the latter being now represented by the gneissic granite to
be found on the south of this ridge, and by the gneiss, etc., occurring on both

sides of it.

2. Numerous varieties of gneiss occur within the Pre-Cambrian area, some of
which will be briefly described in a separate paper dealing with the microscopic

characters of these rocks.

Specimen No, 29 represents a very typical variety of gneiss occurring in the
McDonnell Ranges. It is strongly foliated, but the folia, which usually have a
thickness of from quarter to half inch, are not very persistent. They pinch out,
occasionally very rapidly forming lenticular masses, which usually in this variety
are much drawn out. These lenticular masses are sometimes, however, very short
and ‘“‘eye”-like. The folia, which consist for the most part of quartz, felspar (a
great portion of which is a plagioclase with low angles of extinction), and a few
grains of biotite, are separated from one another by thin black layers of biotite not
more than one-eighth inch thick. These thin layers of biotite are usually roughly

parallel to one another, but occasionally they intersect.

HORN EXPEDITION

GENERAL GEOLOGY. 43

Specimen No. 97 is an example of a gneiss which exhibits a more advanced
stage in the production of “eyes” than that just described. This variety of
gneiss, which was met with on the north side of Brinkley Bluff, was observed to

extend over a large area in the McDonnell Ranges.

In this specimen the felspar and quartz are not so distinctly marked off into
folia separated by thin more or less parallel layers of biotite. They seem, however,
to be much crushed, and, together with the biotite, to form, as it were, a ground

mass to the lenticular portions.

These lens-shaped masses usually show when examined carefully their relation
to the remainder of the rock, by the presence of narrow Jaminal running out from

them into the mass of the rock.

Another specimen (No. 4) seems to mark a further stage in the process of
metamorphism ; it was obtained from an outcrop in the bed of Maude Creek,
which takes its rise on the southern slope of Hart Range, and is a typical

representative of a gneiss found extending over a large area.

The finely-foliated structure is not so well marked in it as in the above-
mentioned specimens. There seems to have been a greater movement of the
constituents during crushing, the fine portions of which wrap round the lenticular
masses in such a manner as to simulate the ‘ flow-structure” so well developed in

many volcanic rocks with porphyritic crystals.

The “eyes” are entirely isolated, and consist chiefly of quartz and felspar,

while in the ground mass are to be seen quartz, felspar, biotite, and garnets.

A gneiss from Belt Range (No, 34) resembles in structure specimen No. 4.
In the former, however, the “eyes” are composed of microcline, and are embedded

in a crushed mass of felspar, quartz, and a small quantity of decomposed mica.
3. Those that are clearly of eruptive origin :—
(a) Rocks of the Acid Group.

“Oolgarna” granite. The granite from which the immense crystals of mica
are obtained, at the Oolgarna Claim in the Hart Range, is composed of the usual
constituents of ternary granite, viz., quartz, felspar, and mica. As the felspar
belongs to the triclinic division, the rock ought to be termed a granitite. Although
all the constituents are developed on an enormously large scale, the crystals being
often from two to three feet in diameter, no one particular mineral is porphy-
ritically developed. The felspar is of two kinds—a potash variety, which invari-

OA

44 HORN EXPEDITION—GENERAL GEOLOGY.

ably exhibits the characteristic ‘‘ cross-hatching” of microcline, and a plagioclase
belonging to the soda end of the soda-line series, with very low extinction angles
and very fine polysynthetic twinning. The mica is also of two kinds, a black
variety biotite, and the potash variety muscovite. | Beryl and tourmaline occur as

accessory minerals.

The granitite from an intrusive dyke on the opposite (western) slope of the
mountain spur to that on which the Oolgarna Claim is situated has an almost
identical mineralogical composition to the Oolgarna rock. There are the same two
varieties of felspar, a microcline and a plagioclase, with well-developed polysynthetic
twinning and small extinction angles. Of the micas, muscovite alone appears to be
developed in this dyke, and hugs in a marked manner its southern wall. Here
also tourmaline and beryl occur as accessory minerals, with the addition of some
small red garnets. A crystal of beryl was obtained from this rock, which measures
three inches in diameter and six inches in length. Its form is that of a perfect
hexagonal prism, the terminal ends of which are not present. It exhibits macros-
copic zoning, the several zones of the mineral having a slightly different tint, with
a central nucleus of quartz and felspar. Its colour varies from pale green to
yellowish green. The plates parallel to the basal plane, obtained by taking advan-
tage of the somewhat imperfect basal cleavage, were found to yield in convergent
polarised light excellent interference figures having a negative sign. Some of the
hand specimens from this dyke consist entirely, or nearly so, of felspar, sometimes
microcline, at other times a soda plagioclase ; others consist entirely of quartz and
muscovite, while yet others again consist entirely of mica. The order of crystalli-
sation, as determined from the hand specimens, is mica, quartz, and felspar. The
felspar has crystallised out last, as it frequently encloses entire crystals of quartz
and mica. The mica has crystallised out first, for where the quartz comes into
direct contact with a crystal of mica its (the quartz) outline is found to have been

determined by that of the mica.

A specimen (No. 93) which was obtained in the McDonnell Ranges, near the
head of Ellery’s Creek, represents a type of gneissic granite, which is not uncommon
in these ranges. There can be no doubt that it is a granite which has undergone
a certain amount of crushing, but not enough to make its origin a matter of doubt.
It consists for the most part of microcline and quartz, which are often inter-
crystallised in a manner similar to that observed in graphic granite. The rock in
the hand specimen does not appear to be foliated, whereas, in the field, a coarse-
banded foliation was observed. Masses of intercrystallised microcline and quartz

are separated by thin irregular laminz of biotite flakes.

HORN EXPEDITION—-GENERAL GEOLOGY. 45

A second specimen (No. 96) is a gneissoid granite from Alice Springs with
large porphyritic microcline erystals. The mass of the rock scarcely exhibits
foliation in hand specimens, but when examined in the field it is found to be
distinctly foliated. It consists of quartz, felspar (microcline), and two varieties of

mica, biotite and muscovite, of which the former is most abundant.

A third specimen (No. 139) is from a dyke intruding gneiss near the head of
Ellery’s Creek. — It consists of grey quartz, muscovite, and a white rather opaque
plagioclase exhibiting very fine twin lamellation parallel to 0°10, and very low
extinction angles. This granite resembles in its mineralogical composition, and its
structure, that occurring on the north side of Hart Range, which latter has
yielded the very largé mica crystals. Many of the gneisses, especially in the
vicinity of intrusive masses, are found to contain epidote, sometimes in large
quantities. The epidote sometimes occupies small veins in the gneiss; at other
times it is found to be present in the form of irregular grains throughout the mass

of the rock.
(6) Intermediate group.

Near the Oolgarna mica-claim a fine-grained intrusive rock occurs, which is,
at first sight, not unlike a basalt, though somewhat lighter in colour. In thin
sections it proves to be a granulitic pyroxene diorite with much hypersthene, and

a fairly large quantity of magnetite and uralitie hornblende.
(c) Basic Group.

Between Slip-panel Gap and Ellery’s Creek a large number of dykes of
basie rocks occur intruded amongst the gneisses, ete. The strike of these
dykes is usually N.W. and 8.E., some of them being traceable on the surface for
long distances. One dyke was observed to be as much as 600 feet in width,
the rock of which it is composed being an olivine dolerite. The basic rock of one
of these dykes proved to be a gabbro (No. 109) consisting of diallage, a plagioclase
with an extinction angle about that of labradorite, and magnetite in large grains.
Another of these basic rocks (Nos. 195 and 179) appears to be an olivine dolerite,
consisting of plagioclase, augite, a considerable quantity of undecomposed olivine,
magnetite, and a few grains of hypersthene. Ophitic structure is well developed,
in which large irregular masses of augite enclose a number of felspar crystals.
Another rock (No. 64) is a diabasic dolerite, in which much of the felspar and
augite is decomposed resulting in the production of epidote, chlorite, fibrous horn-

blende and, perhaps, saussurite.

46 HORN EXPEDITION—GENERAL GEOLOGY.

II1I.—Ordovician.

(a) Introductory.

If the group of metamorphic rocks just described be considered Pre-Cambrian,
then the Cambrian is altogether unrepresented ; and either sedimentation never
took place over the area now exposed, or if it did, the materials so deposited were
entirely denuded off from this area during the long interval separating the con-
clusion of their deposition and the disappearance of this region beneath the waters

of the Ordovician sea.

Messrs. Brown and Chewings, however, have at various times argued, on what
appears to us insufficient evidence, that the age of certain strata flanking the
McDonnell Ranges on the south is Cambrian. Thus Mr. Brown (x., p. 2) in 1890
examined in the vicinity of Heavitree Gap, to the south of Alice Springs, a series
of rocks resting unconformably upon the “Metamorphic and Plutonic Primary
rocks ” of the McDonnell Ranges, and called them ‘“ Primary rocks (Cambrian ?).”
He included in this series ‘“quartzites (sometimes conglomeratic), dolomitic lime-
stone and occasionally clay-slates.” ‘They vary,” according to this author, “in
dip and strike, are often much twisted, contorted, and dislocated. . . . And
the granite and other dykes and quartz reefs do not extend into these rocks, nor

have fossils been observed in this formation.”

In 1891 Mr. Chewings (xi., p. 249) did not include Cambrian in his classifica-
tion of the rocks of this district, the rocks of Mr. Brown’s Cambrian being partly
included by Mr. Chewings in his Pre-Silurian, and perhaps partly also in his

Silurian.

In the same year Mr. Brown (xii., pp. 12, 13) says :—“ Lying unconformably
on the crystalline, metamorphic, gneissic, and granitic Archean rocks of the
McDonnell Ranges, there are two other rock systems unconformable to each other.
The lower of these two systems,” he continues, “consists of quartzite, quartzite
conglomerate, dolomitic limestone, limestone, sandstone, and slate, striking east
and west. They are lithologically similar, and doubtless of the same age as the
quartzite, dolomitia limestone, limestone, sandstone, and slate series of the Flinders
and other ranges in the northern part of South Australia proper (in the limestone
of which fossils of Cambrian age have been identified by Mr. Etheridge . . . ),
the Dennison and Peake, Mount Dutton, and ranges to the west of the Musgrave

”

and in the neighbourhood of Mount Burrel.

HORN EXPEDITION—GENERAL GEOLOGY. 47

Tt is unfortunate that Mr. Brown gives no account of the evidences of the
unconformability between this series of rocks and his upper system, which contains

fossils determined by Mr. Etheridge to be Lower Silurian.

In the following year Mr. Brown (xiv., p. 7), again classifies the quartzites,
dolomite, limestone, sandstone, and slate, which overlie the Pre-Cambrian rocks
unconformably, as Cambrian. He includes in his Cambrian series the rocks
occurring between Mount Sonder and the northern boundary of the alluvial plain
of the Finke, north of the Lutheran Mission Station. There is also on p. 11
a geological sketch-section showing the relations of the rocks of Mr. Brown’s

Cambrian system to those above and below.

Two sets of observations made by us prove fatal to Mr. Brown’s establishment
of a Cambrian System in Central Australia. The first is the presence of fossils of
Ordovician age occurring in a dense grey quartzite and in a reddish argillaceous
limestone (ude Section McDonnell Range to Levi Range), almost identical with
that found on the north side of George Gill and Levi Ranges, and recognised to be
Ordovician by Mr. Brown. The quartz-grits also associated with limestone at
Deep Well, and both limestones and associated gritty sandstones at Chandler’s
Range contain Ordovician fossils. The second is the discovery of water-worn
fragments of the red Ordovician limestone containing characteristic fossils in the
uppermost portion of the immense bed of conglomerate and conglomeratic sand-
stone, which overlie the quartzites and limestones of Ordovician age (v/de Section
McDonnell Range to Levi Range), and which form the northern boundary of the
Missionary Plain, north of the Lutheran Mission Station. The red argillaceous
limestone, mentioned above, was found outcropping on the northern side of Horn
Valley, which is a longitudinal valley of great length separating two quartzite
ridges. The actual locality where this fossiliferous limestone was observed is
situated ten miles west of the Finke Gorge. The limestone, charged with Ort/is
leviensis, was observed to be dipping to the north at a very steep angle, and to be
overlain by quartzite. It was in this quartzite, at a point a few hundred yards
south of the northern end of the Finke Gorge, that “doceras and other Ordovician
fossils were also found. Thus in the very centre of Mr. Brown’s so-called
Cambrian System, and in rocks forming an important part of it, Ordovician fossils

have been found.

The second piece of evidence determines, without a doubt, the age of the
conglomerate, also included in Brown’s Cambrian System, to be not Cambrian but
Post-Ordoyician. In view of the evidence just mentioned there can be no doubt

that we are perfectly justified in considering the strata (excepting the Post-

48 HORN EXPEDITION—GENERAL GEOLOGY.

Ordovician conglomerate) as far north as the northern edge of the Finke River
Gorge as Ordovician. To what system the strata, that lhe between this point and
Mount Sonder, belong we have no paleontological evidence to show. Owing to
the absence, however, of any signs of unconformability, we are of opinion that
they belong to the Ordovician System. There does not appear to be a great thick-
ness of strata on the south of Mount Sonder, as an inher of gneissic granite
belonging to the Pre-Cambrian system is visible in the valley of the Davenport.
The rocks composing Mount Sonder and the low hills to the south consist of
quartzite, micaceous slates, and dolomitic limestone highly altered by the earth
movements, which seem to have been greatest here, and to have decreased in force
southwards. For this reason these rocks appear more altered than the typical
Ordovician rocks further south. We therefore cannot adopt Mr. Brown’s classifi-
cation, because we have undeniable evidence of the Post-Ordovician age of one
part and of the Ordovician age of another, and lastly, because no reliable evidence
has been furnished of the Cambrian age of the remainder. Rocks of Cambrian
age constitute a large part of the Flinders Range, being certainly known to be
developed as far north as the Ajax Mine, between Beltana and Leigh’s Creek,
where fossils similar to those found at Parachilna, Blinman, and other localities
in the Flinders Range, and described by Mr. R. Etheridge, Junr., have been

discovered.

n Ip. wings (XvV., p. in nat annelid burrows are
In 1894 Mr. Chewings (xv., 198) pointed out that annelid |
present in the quartzites on the north side of Mereenie Bluff, and considers that
these rocks may be Cambrian. Similar annelid burrows were found by us in a
quartzite range, which appears to be an eastern extension of that spoken of by Mr.
Chewings. Some of the quartzite yielded to us other fossils, which fix its age as
rdovician, and no doubt determine the age re ridge referred to b te
Ord ; 1 loubt det the age of the ridge referred to by M
Chewings to be also Ordovician. In the same paper Mr. Chewings includes under
his heading Cambrian and Pre-Cambrian (?) the rocks occuring in the valley of the

Davenport. Our reasons against such a view have just been given.

In 1889 Mr. Brown (ix., p. 2) described the occurrence in the vicinity of
Mount Burrell of limestone with flinty veins, quartzite, sandstone, and slates,
which he judged, basing his conclusions on lithological evidence, to be of the same
age as his so-called Silurian rocks of Anna Creek and Finnis Springs. These
latter bear every appearance of being northern inliers of the series of rocks, which
constitute a great portion of the Flinders Range, and which, at least as far north
as the Ajax Mine, have been lately proved on paleontological evidence to be
Cambrian. There is no doubt that the Mount Burrell strata belong to the

HORN EXPEDITION—GENERAL GEOLOGY, 49

Ordovician System of rocks so strongly developed to the north of Mount Burrell
and between this point and the McDonnell Ranges, and which have now yielded

Ordovician fossils in so many localities.

In this report Mr. Brown distinguishes an overlying series “composed of
brown and white sandstone in horizontal and inclined layers,” and called by him
Devonian (?); but as this author in a later report (xiv., p. 7) relinquishes this

division, it will not be necessary to make any comment.

In his topographical description of the country lying between the Flinders
and MeDonnell Ranges, Mr. East (vii, p. 31) treats the subject under three
headings, viz., (1) “The Great Austral Plain,” (2) “The Terraces,” and (3) “The
Great Central Plateau.” Had Mr. East divided this area geologically into three
corresponding divisions, the rocks of each belonging to one of the geological
systems, he would have made an approximation to the truth. If he had called
the rocks occurring in the area included in his first topographical division Cre-
taceous, those of the second Silurian, and those of the third Pre-Cambrian, he
would have given an infinitely superior geological classification than that suggested

by the following statement (vii, p. 51) :—

“With regard to the geological age of this region” (between Lake Eyre and
Everard Plain on the north side of the McDonnell Ranges) ‘the presence of fossils

on the face of the slope up to an altitude of 800 feet”

(referring probably to the
discovery by himself of Lingua subovalis at Mount Daniel) “places us on pretty
sure ground and shows the age of deposition to be Mesozoic, and probably Cre-
taceous. Farther up the slope there must exist doubt until fossils are actually
discovered, though it is a reasonable presumption that the beds throughout belong

to one great series.”

In criticising this statement it must be borne in mind that it was not until
two years after the publication of Mr. East’s paper that Lower Silurian fossils
were first described from Central Australia. After making due allowance,
however, for the absence of paleontological evidence to the north of Mount
Daniel, it is difficult to understand how any geologist, who had travelled over the
Cretaceous, Silurian, and Pre-Cambrian rocks, could formulate such a theory. The
rocks of the three systems under consideration differ from one another in litho-
logical characters and structural features as much as it is possible for any three
sets of rocks to do, Not only so, but the change in these features is sudden and
well-amarked, even though the actual junction-line itself be not observed. Thus
the Cretaceous rocks have very characteristic lithological characters, and dip at

‘

50 HORN EXPEDITION—GENERAL GEOLOGY.

extremely gentle angles (usually at an angle of not more than two to three degrees)
throughout the area occupied by them; while the Silurian rocks, consisting of
sandstones, quartzites, and limestones, unlike the Cretaceous, dip at from 40° to
50° in the vicinity of the junction-line of the two formations. Again, on leaving
the Lower Silurian area at Heavitree Gap, for instance, the differences, both litho-
logical and structural, to be observed in the two sets of rocks ought to attract the

notice of even the most casual observer.

In 1890 Mr. Brown (ix., p. 6) placed the quartzites, dolomitic limestone, and
clay slates, which are seen to rest unconformably on the Pre-Cambrian rocks at
Heavitree Gap and elsewhere, and which appear to be unclassified in the sketch
section accompanying his previous report, in a group by themselves, which he calls
Primary rocks (Cambrian ?). Ona study of Mr. Brown’s later reports (xiv. p. 7)
it will be observed that he retains this division, but extends the area of the rocks
included in it as far south as the Lutheran Mission Station, absorbing thereby
part of his former Silurian rocks. In 1891, after the determination of the Lower
Silurian age by Mr. R. Etheridge, Junr., of the fossils submitted to him by Mr.
3rown, his (Mr. Brown’s) original Silurian became Lower Silurian, and, as more
clearly stated, was made to include the rocks of the George Gill, the James, and
Ooraminna Ranges. Thus the rocks which in 1890 were classified as Devonian (?)

are now included in the Lower Silurian.

In 1891 Mr. Chewings (xi., pp. 249-252) called a portion of the system of
rocks under consideration Silurian, basing his classification on the determination
of the Silurian age of the fossils collected at the head of the Walker River, at
Mereenie Bluff, and on the Petermann Creek. This author separates from this
system the Ooraminna sandstone and the conglomerate which flanks the South
McDonnell Range. The Ooraminna sandstone, as there is every reason to believe,
belongs to the Ordovician system, but we have positive evidence of the Post-
Ordovician age of the conglomerate.

In a note to this paper of Mr. Chewings’s, Prof. Tate (xi, p. 255) gives a list
of the fossils identified by him, and from the meagre evidence afforded by them
was inclined to assign an Upper Silurian age to them. Mr. Chewings’s Devonian
of the George Gill Range is identical with the red sandstones overlying the fossil-
iferous Ordovician limestones, which sandstones have there a very low dip, but are,
nevertheless, superimposed conformably on the limestones, which outcrop in
Petermann Creek (vide Fig. 7). The Tertiary deposits of the same author are

outliers of the same range, which, because of the low dip and the fact of their

HORN EXPEDITION—GENERAL GEOLOGY. 51

being seen from the south in their strike-plane, present the appearance of an

unconformable capping.

In 1891, in his paper entitled ‘ Descriptions of some South Australian
Silurian and Mesozoic Fossils,” Mr. R. Etheridge, Junr.,* described the following
Lower Silurian fossils :—Raphistoma brownit, Orthoceras sp. ind., and Orthis
leviensts. In a note in the same report Mr. Brown describes the discovery of these
fossils in September, 1890. In this report, and two subsequent ones, Mr.
Etheridge assigned the fossils to a Lower Silurian age. A complete account of

the fauna will be given in Part V.—PsLmonro.oey.

As has been mentioned already, we eliminate Cambrian from our classification
of the rocks occurring within the region under consideration (from Oodnadatta to
the McDonnell Ranges) for the reasons that have been detailed. We include in
the Ordovician system all the strata lying between Mount Burrell Cattle Station
on the south and the McDonnell Ranges on the north, with the exception of the
conglomerate which was observed on the north side of Rudall’s Creek, and on the

banks of Ellery’s Creek north of the Lutheran Mission Station (Hermannsburg).
(0) Extent.

In the journey north from Oodnadatta the first outcrop of Ordovician
strata was seen about seven miles north of Francis Well on the Hugh River,
and about the same distance south on the Mount Burrell Cattle Station,
which is also on the Hugh. The southern boundary of the Ordovician area
extends westerly from this point, passes a few miles south of Chandler’s Range,
and thence sweeps round the southern faces of Levi and George Gill Ranges, and
perhaps continues for many miles further west. Hast of Mount Burrell the
southern boundary is not known. The northern limit of this area is partly formed
by the prominent quartzite ridge, in which are the Heavitree, Emily and Jessie
Gaps ; but at Mount Sonder, and to the west of it, there are beds which intervene

between this quartzite and the Pre-Cambrian rocks.

The above-mentioned ridge is traceable for about twenty-five miles east of the
first-named gap, beyond which it sweeps suddenly northwards; so that in
journeying due east we find the Pre-Cambrian rocks overlain by a northern
extension of the Ordovician strata. The northern boundary of the Ordovician
rocks north of Mount Benstead, and east of that point, has not been traced. In

journeying nearly due east of Mount Benstead, and at a distance of about twenty-

* Reports on Coal-Bearing Area in Neighbourhood of Leigh’s Creek, Adelaide, Ls91, pp. 9-14, pl. i.-ili.
7A

Md

52 HORN EXPEDITION—GENERAL GEOLOGY.

eight miles from that place, the track emerges from the Ordovician Ranges,
through which it had led for that distance, on to Pre-Cambrian gneiss. To the
north, from two to three miles distant, a somewhat elevated quartzite range is to
be seen forming, in all probability, an outlier of Ordovician strata. To the south
another quartzite range was seen, which probably constituted the northern limit of
the main Ordovician area. Between these two ranges the Ordovician strata have
been entirely removed, exposing the Pre-Cambrian rocks at the surface, which
have been eroded into characteristic low, rounded, “jumbly” hills. Eastward
from this last point the Ordovician rocks lie wholly to the south, the northern

quartzite range dying out after a short easterly course.

At Arltunga (Paddy’s Hole) the northern boundary lies a mile or two south

of the mining township, its further eastern course is not known.

Westward of Alice Springs the quartzite ridge, which marks the northern
limit of the Ordovician strata, continues to Mount Gillen, where it sweeps 8.S.W.
(about). In this face is an opening known as Temple Bar Gap. The range
continues a,short distance south of this opening, and then turns westward past
Burt’s Bluff; still further west it continues to Mounts Sonder and Zeil, and Belt
Range. The western boundary of this area is not known; but judging by the
observations of Mr. Tietkens, these rocks extend across the West Australian
border.

(c) Stratigraphical Relations.

The lowest stratum of the Ordovician System found directly overlying
the Pre-Cambrian gneiss a few miles to the south of Alice Springs is a dense
grey quartzite (wide Fig. 26). The junction-line between this quartzite and
the gneiss, where not concealed by a talus of quartzite, is seen to be uneven,
and more or less undulating; a fact which, coupled with the great funda-
mental differences of a lithological and structural character, evidently points to the
presence of a strong unconformability, separating these members of the Ordovician
and Pre-Cambrian Systems. The same features are seen in Belt Range, as indi-
cated by Chewings (xi.) at Haast Bluff, but not Haast Bluff of Giles. Here
friable gritty sandstones and quartzite, aggregating 1500 feet in vertical thickness,
repose in an east and west direction on an undulating surface of schistose rocks,
and over which they transgress in a south and north direction (see Fig. 3 and
Section from Mereenie Bluff to Belt Range). Similar appearances are presented
in Mount Zeil, as seen from a distance of three-and-a-half miles; here a crown
of quartzite transgresses over schistose rocks, which have conspicuous planes of

foliation dipping north at a high angle.

HORN EXPEDITION—GENERAL GEOLOGY. o3

At Gills Pass the Ordovician limestones, dipping south, come into contact
by a fault with a glassy quartzite (forming a high, scarped ridge), which introduces
the Pre-Cambrian rocks, which continue uninterruptedly northward to Burt Plain
with high planes of foliation dipping north (see Section from Missionary Plain to
Gill’s Pass), Although the actual junction line was not observed, there is strong
evidence that the Ordovician limestone and quartzite and the Post-Ordovician
conglomerate, already referred to, are unconformable to each other. In the lowest
strata of this conglomerate among pebbles of other rocks were found waterworn
fossilifcrous fragments of the red crystalline limestone belonging to the Ordovician
System. Thus the Ordovician limestone must have been consolidated, upheaved

above sea-level, and eroded before the formation of this conglomerate.

The actual junction-line between the Ordovician and the Cretaceous was not
observed. The great difference in the amount of dip of the strata of the two
systems, even close to the junction, as observed a few miles south of Henbury
Cattle Station on the Finke, gives some idea of the strong unconformability that
must exist between the rocks of the two systems. At Henbury itself small outliers
of horizontally bedded chalcedonized sandstone, so characteristic of the Cretaceous,
rest on Ordovician argillaceous limestone, dipping at a moderately high angle to
the south-east, the actual contact being concealed by the waste from the overlying

bed.

(2) Structural Features.

Folding.--The Ordovician rocks have been thrown into a number of
folds, gentle in the south as in the George Gill and Levi Ranges, and
becoming sharper in the north. In the ranges just mentioned the rocks,
chiefly sandstone, dip at low angles, viz., from 8° to 10° to the south on the north
side, and about the same amount in an opposite direction on the south side. Thus
the rocks of these ranges form a shallow synclinal trough ; the corresponding arch,
probably originally situated on the north side of these ranges, has been entirely
removed by denudation and erosion, its place being now occupied by the valley of
Petermann Creek. At Mount Sonder and in the valley of the Davenport to the
south, at the opposite edge of the Ordovician area, the strata have suffered the
greatest amount of disturbance. There quartzite, alternating with micaceous shale
and passing below into dolomitic limestone, is dipping at high angles to the north

(see Section McDonnell Range to Levi Range).

Absence of Eruptive Rocks. —S somewhat remarkable feature of this ancient

system of rocks is the total absence, as far as observation goes, of eruptive rocks,

54 HORN EXPEDITION— GENERAL GEOLOGY.

whether plutonic or volcanic. There is no evidence either of the presence of
intrusive dykes or sills, or of interbedded lavas or tuffs throughout the whole area

examined.

False-bedding.—False- or current-bedding is strongly developed in the sharp
gritty sandstones at Glen Edith, and on the north side of the range which forms
the southern boundary of Shake’s Plain, which is known locally as the Station Range,
situated on the south side of Tempe Downs Cattle Station. There the current-
bedding is so well developed that one is apt at first sight to mistake the false-
bedding planes for the true-bedding planes. The former, however, are seen to
vary so rapidly in the direction of their dip that the mistake can be easily rectified,
and the true bedding planes made out without much trouble.

Ripple-marks.—Vhe surface markings known as_ ripple-marks are well
exhibited by the sandstone constituting the Levi and George Gill Ranges. In
the Levi Range, where they were particularly noted, the alternating ridges and
furrows were seen to have a very varying trend, at one time ina N.W. and 8.E.
direction, and at another in a N.N.E. and 8.8.W. direction. The width of the
ridges, as also of the furrows, was about one inch, and the height from the bottom
of the furrow to the crest of the ridge about half an inch. In George Gill Range,
where ripple-marks were seen to be extensively developed, the sandstone is evenly
and thinly bedded, and the surfaces of many succeeding lamin were seen to be
ripple-marked. The evidence deduced from the presence of these ripple-marks
indicates shallow water deposition of the strata in which they occur ; that is of
the sandstone of George Gill and Levi Ranges. Ripple-marks were also observed
in the quartzite forming the walls of Heavitree Gap, and in the quartzite near the

northern extremity of the Finke Gorge.

Concretionary Structure.—Concretionary masses composed chiefly of hydrated
oxide of iron occur in the fossiliferous limestone on the south side of George Gill
Range. Concretions of a siliceous nature were observed in the siliceous limestone
flanking the Mount Gillen quartzite ridge on the south. A concretionary lime-

stone was also observed in the Finke Gorge.

Sedimentation in Relation to Physiographic Changes.—A natural cycle of
sedimentation bearing a definite relation to the physiographic changes, through
which the locality under consideration has gone through, can be made out in
certain portions of the Ordovician strata. The northern half of George Gill
Range, for instance, is composed of sandstone dipping to the south. This is

followed on the uorth in regular descending order by calcareous shales or, perhaps

HORN EXPEDITION—GENERAL GEOLOGY. 975)

more strictly, by soft argillaceous limestone, and this by hard red limestone
comparatively free from argillaceous matter, and this latter by a great thickness of
sandstones and quartzites. The lowest strata, and those first deposited, bear
indications of shallow water deposition, probably on a sinking sea-bottom. The
next strata, the limestones, point to deeper water conditions and practical
quiescence, although the water still remained muddy, as evidence by the some-
what argillaceous character of the limestone, and by the presence of trilobites and
rarity of corals. The strata next in ascending order indicate upheaval and
deposition in shallower water, these strata being much less calcareous and more
argillaceous than the preceding limestone. Lastly, on top we have a great thick-
ness of sandstones, the uppermost layers especially, which are rippleamarked to
such a great degree, and which contain pebble bands, as in the Glen of Palms,

Laurie’s Creek, etc., pointing to deposition in very shallow water.

Dip.—The strata of the Ordovician system dip at very varying angles. Asa
general rule, however, it may be said that the dip increases as we go northwards.
This has its explanation in the more highly-disturbed state of the rocks in the
northern portion of this area. The three following series of observations on the
dip of the strata will give some idea of the steady increase in the angle of inclina-

tion of the strata in a section across one arm of a fold :—-

1. Levi Range northwards for a distance of about four miles 9°, 14°, 14° 30%,

ie, 22°, and 37”.

2. From Bowsen’s Hole in a N.W. direction. At Bowsen’s Hole the dip was
10°; at 3 miles was 15°-— 20°; at 4, 30°; at 6, 35° 40°; at 63, 45°-50°; at 8,
70°; at 84, 75°; at 14, 80°.

3. At the western extremity of the Mereenie escarpment, which constitutes the
wall-like southern boundary (rising to nearly 1000 feet) of Horn Valley, the dip of
the fossiliferous limestones is 37° 8. 5° W. At the entrance to Stoke’s Pass (three
miles due north) the dip of the quartzite, which forms the northern wall of Horn
Valley, was found to have increased to 60°; and that of the underlying beds to

increase still further to their northerly termination.

(e) Detailed Sections.

1. Section through Levi and James Ranges (z/de Section McDonnell
Range to Levi Range). A traverse across Levi Range revealed the fact
that the sandstone composing this range has the form of a shallow synclinal

trough, Levi Range has a steep escarpment on its north and south faces

56 HORN EXPEDITION—-GENERAL GEOLOGY.

from three to four hundred feet high. The dip of this sandstone varies from
6° to 8° on the north and south faces of the range, while about its centre the
dip changes, within the distance of half a mile, from 4° 8.8.W. to 4° N.N.E. On
the summit of the northern escarpment the sandstone exhibits well-marked false
or current bedding, and the surfaces of the strata are ripple-marked. This sand-
stone, which as a rule is fairly indurated and often approaches a quartzite, in other
places is of a white friable felspathic nature, indurated in places by secondary
silica. No fossils were discovered in this sandstone. Underlying this is a
yellowish thinly-bedded indurated mudstone, with more or less perfect cubes on
the weathered surfaces, which may represent pseudomorphs after some mineral,
probably rock salt. The cubes vary from about an eighth of an inch to over half
an inch in diameter, the faces being concave. Underlying this latter rock quite
conformably are the fossiliferous limestones, which have yielded a small number
of Ordovician fossils. This limestone varies much in character when traced in the
direction of its strike for any distance. It is, however, always very argillaceous,

and varies from a grey to a yellow and very often red colour.

On the north side of Levi Range it dips at an angle of 14° 8.S8.E., and appears
to be quite conformable to the sandstone of the range. It has yielded numerous
specimens of Ovthoceras and Eundoceras, besides many specimens of Raphistoma
browntt. The same series of rocks are to be made out to the west of Levi Range.
In the George Gill Range the sandstone has most of the characters exhibited by
the same rock in Levi Range, with the addition of a finely-bedded structure, well
seen in Martin’s Pass.

The uppermost zone is very rich in Orthis leviensis, while below come beds
enormously rich in Trilobite fragments. Quartzites underlie these limestones on
the north, the uppermost strata being apparently unfossiliferous. They dip at 14°
(about) in a 8.S.W. direction, and are succeeded a little further north by fossili-
ferous quartzites dipping 17° 8S.S.E. The total thickness of Ordovician strata
between Levi Range and the point to the north of it, where the dip becomes
reversed about three-and-three-quarter miles north of Camp 25 on the bank of
Petermann Creek, is 7000 feet.

At the top of the series are 560 feet of red sandstone, exhibiting current-
bedding and ripple-marks. Levi and George Gill Ranges are composed entirely of
this rock. Below this come 440 feet of yellow and grey mudstones and earthly
limestones and yellow and red argillaceous limestones, in the lowest beds of which

the majority of the fossils have been found. Lastly, below the limestones there are

HORN EXPEDITION—GENERAL GEOLOGY. 57

6000 feet of sandstones and quartzites, some small part being composed of thinly-

bedded, highly argillaceous sandstone, passing into red micaceous clay shale.

Fossils were found in the quartzite about half a mile north of Camp 25 on
Petermann Creek, and again at two-and-a-half-miles north of the same point.
Further north still, on the northern half of this great denuded anticline, the fossili-
ferous horizon in the quartzite was again met with ; while still further in the same
direction, near Tempe Downs Station, the fossiliferous limestone, on the same
horizon as that mentioned above, comes to the surface, and has yielded many

fossils.

A vertical section of the fossiliferous beds in Middle Valley at Tempe Downs
is as follows :—
Thickness.

Three hands of fossiliferous limestone, from two to four inches thick,

dipping at 80° to the south, separated by sandy clay-slates - 45 feet.
Sandy clay-slate, charged with Asaphus tlarensts, passing into - : Sere
Soft sandstones crowned by a quartzite, which is fossiliferous - =O ee

2. Ooraminna Pass Section.—The Oooraminna Range, which has a breadth of
seven miles, is intersected in a north and south direction by a narrow valley
excavated toa depth of from 200 to 300 feet. The basal rocks are bluish-grey
dense limestones in courses of two to four feet thick, separated by thinner fissile
limestones. They strike W. 10° N. and dip from an anticlinal ridge at 9° ; a total
thickness of forty feet was measured in the limestone series. In distinct conforma-
bility there succeed quartzose sandstone and two chief quartzite bands, the
uppermost of which forms the chief surface-rock of the range (see Section 8). No
fossils were observed, but a hard yellow sandstone forming part of the corres-
ponding arenaceous series in James Range, penetrated in the well-sinking at
Deep Well, contained casts of Zscarce. Limestones similar to those of the
Ooraminna Pass, and readily recognisable by their exceedingly hackled weathered
surfaces, form the superstructure of the country from James Range to the southern

boundary of the Ordovician area,

The quartzites of the Ooraminna Pass are somewhat irregularly developed,
and occasional instances were observed, particularly at Ooraminna Waterhole, of
the gradual passage in a horizontal direction from sandstone to quartzite. A
remarkable physiographic feature is presented at the south escarpment of the
range in the form of four or five tall, wall-like masses of quartzite in close
proximity (locally known as Hell Gates), The planes of stratification in the

8

58 HORN EXPEDITION—GENERAL GEOLOGY,

adjacent sandstones are distinctly traceable, the dip not exceeding 10°. These
structures must have resulted from silicification passing downwards along vertical
planes of limited width, so that alternations of quartzite and unaltered sand-
stone occur, and that subsequent denudation has removed the softer intervening

material.

3. Red-bank Gorge Section.—A section of the strata exposed in the gorge,
through which the Red-bank Creek finds its way through the range, was examined,
together with the exposures to the south. The strata here are much disturbed and
altered, and the bedding-planes of the quartzite, in which for the most part the
gorge has been cut, can only be made out with great difficulty. Further south the
quartzite gives place to micaceous clay-slate, the junction line between the two
rocks revealing the amount and direction of dip. Bands of much-crushed quartzite
and clay-slate, dipping at an angle of 32° N.N.E., alternate with one another as
we travel southwards. At the southern extremity of the gorge the quartzite is
entirely replaced by micaceous clay-slate, which is in places highly charged with
oxide of iron, and some part of which is no doubt identical with the ironstone hill
described by Mr. Tietkens (xi, p. 10). Underlying this clay-slate are thick beds
of much-disturbed and contorted magnesian limestone containing large concre-
tionary masses of oxide of iron. White masses of magnesite, which have weathered
out of the limestone, occur on the surface. Interbedded with this limestone are
thin bands of a strongly-laminated yellow micaceous shale. The limestone has
been much cracked, and into the usually narrow crevices thus produced anhydrous
and hydrous varieties of silica have filtered, forming numerous veins, which inter-
sect the limestone in an irregular manner. Further south the surface of the
country is covered by sand, gravel, and river-alluvium of the Davenport and its
numerous tributaries.

In the valley of the Davenport, west of Mount Sonder, gneissic granite was
observed outcropping at the surface, being in all probability an inher of the Pre-
Cambrian group. In the range through which the Finke River flows (when there
is any running water in its channel) quartzite occurs shortly below the junction of
the Ormiston and the Davenport, dipping at very high angles to the north.
Further south along the Finke Gorge fossiliferous quartzite succeeds, dipping 70°
N. 20° E., this being underlain by thinly-bedded and ripple-marked quartzite, and
by quartzite with annelide burrows. Below this latter we find silicio-argillaceous
limestone passing into quartzite, and further south still there are grey quartzites

dipping 66° N. 20° E,

ae ee se

HORN EXPEDITION— GENERAL GEOLOGY. d9

Observations made further to the west in the Horn Valley prove that red
- fossiliferous limestone underlies the last mentioned rock. South of this last point
there is a great thickness of quartzite dipping at high angles to the north. This

is overlain unconformably by a thick bed of conglomerate of Post-Ordovician age.

The section in Mereenie Bluff presents the following succession of beds in

descending order ; the thicknesses are by estimate :

Thickness.
Quartzite - : e : 7 = : = : = : - 300 feet.

Yellow friable sandstone © - : 5 : : - : = - 300 ,,
Dark brown or purple shales with intercalations in the lower portion
of blue, calcareous, arenaceous shales up to 7 feet thick — - - 100 ,,
Calcareous shales with many thin limestone-bands, the upper ones with
Lsoarca, the lower ones with Orthts leviensts - - - - 60) ,
Unseen — - - 2 - - - - - - - - -

Quartzite forming the south escarpment of Horn Valley.

For general stratigraphical features see Section from Mereenie Bluff to Belt

Range.

(/) Lsolated Portions of Ordovician.

The most southern isolated mass of Ordovician rocks examined by us,
with the possible exception of Ayers Rock and Mount Olga, was a quartzite
hill, which Mr. Winnecke named Mount Watt, and which is situated about
twenty-four miles west of Engoordina on the Finke. This hill, together with
a more elongated mass lying to the north of it, which there was no time to
examine, 1s situated well within the area occupied superficially by rocks of
Cretaceous age. From its summit the flat-topped hills, so characteristic of the
Cretaceous formation, could be seen on all sides; while immediately surrounding
it red sand-hills clothed with Zivod/a formed the prevailing feature, and swept
almost up to its base. This hill, which rises to an elevation of 240 feet above the
surrounding sand-hills and 1300 feet above sea level (according to Mr. Winnecke’s
calculation of the altitude of Camp 14 at the foot of the hill), is composed from
base to summit of a hard, dense quartzite, with a talus of the same material sur-
rounding its base. The strike of the quartzite varies from N. 50° E. to N. 60° E.,
and the dip varies in amount from 7° to 10°. The greater part of the quartzite is
of a grey colour, but there are a few red ferruginous bands, one about six feet and
another fourteen feet from the summit, the latter band having a thickness of
twenty-five feet. The rock is much fissured, one set of cracks running nearly

parallel with the strike.

60 HORN EXPEDITION-—GENERAL GEOLOGY.

Fossils were found in large numbers in this quartzite at and near the summit,
but they were all in the form of casts. The lowest point at which they were
obtained 77 szta was about twenty feet from the summit. Fragments, however,

were found lower, but only in the talus.

Winnall’s Ridge and the outcrops between tt and George Gill Range.—In the
journey from George Gill Range in a 8.8.W. direction to Ayers Rock a number of
outlying portions of Ordovician strata were met with, surrounded on all sides by
red sand-hills. About three-and-a-half miles from Reedy Hole, on the south side
of George Gill Range, the eastern extremity of a low sandstone outcrop was passed ;
at eight miles from the same point a low sandstone ridge with an E. and W. strike
was crossed ; and at eleven miles our course led us past the eastern extremity of a
low sandstone range, striking in a W.N.W. and E.S.E. direction, the sandstone of
which had a dip of about 10° to the south. <All these outcrops of Ordovician
strata are separated from one another, and from those about to be mentioned, by
red sand-hills, which entirely conceal from view the rocks which underlie them.
At twenty-four miles from Reedy Hole a low sandstone range, striking in a W.
35° N. direction was passed, and at thirty-one miles we journeyed within four

miles of an elevated, isolated hill lying W.N.W. of our track.

The last and most important development of Ordovician rocks observed on
the trip to Ayers Rock was Winnall’s Ridge, situated thirty-nine miles 8.8.W. of
Reedy Hole, and nine miles north of Lake Amadeus at the point where we crossed
it, generally known as “ Gosse’s Crossing.” This ridge rises to an elevation of 200
feet at the eastern end, where it was examined, and at the western end it appeared
to rise at least 100 feet higher. Its altitude above sea-level is probably from 1700
to 1800 feet. The strike of the ridge is W. 15° N., and its Jength about three
miles, its width at the base varing from 200 yards to a quarter of a mile. It is
composed of a dense grey quartzite, which on the northern face is observed to dip
southerly at about 25°, and on the south face to dip northerly at about the same
angle. The rock thus forms a synclinal trough, which fact is readily apparent
when the ridge is viewed in the direction of the strike. No fossils were found in

this quartzite.

I1V.—Post-Ordovician Conglomerate.

The earliest reference to this formation is by Giles (iv., p. 17), and was
later traced by Chewings* west of Ellery’s Creek to the head of Rudall’s Creek.

* The Sources of the Finke River, by Chas. Chewings, Adelaide, 1886, pp. 23 and 34.

HORN EXPEDITION—GENERAL GEOLOGY. 61

In 1891 Mr. Chewings (xi, p. 252), classed this conglomerate with ‘ Mudstone
and the Ooraminna Sandstone” as Devonian (7) The Ooraminna Sandstone, as
mentioned elsewhere, we believe to belong to the Ordovician System, whereas it 1s

quite certain that the conglomerate must be younger.

During a trip from the Lutheran Mission Station, on the Finke, northwards
via Ellery Creek to the McDonnell Ranges, an excellent section of this conglom-
erate was examined. Four iniles N. 60° E. from the Mission Station loose pebbles,
that did not appear to be derived from a recent river gravel, were observed on the
surface of low circular hills. Two miles further north a well had been sunk in
micaceous conglomeratic sandstone. Twelve miles N. 56° EK. from the Mission
Station the track crossed Ellery Creek, and here the conglomeratic sandstone was
first seen cx situ, its dip being 15° nearly due south. Further to the N.E. the
conglomerate, alternating with pebbly sandstone, dips at 14? S.8.W., the former
being very coarse in places, some of the pebbles being as much as one to two feet
in diameter. — Here some pebbles were collected, which proved on examination to

eneisses and schists of various kinds, with also a

have been derived from granites, g
few quartzite pebbles. Northwards the angle of inclination of the beds gradually
increases, as the following figures show :—Dip where first observed (at ‘Sheep
Camp”), 15°; at 3 miles, 20°; at 49, 30°; at 6, 45°; at 62, 49°; at 77, 60°;
at 8, 60°.

At eight miles from the locality, where the conglomerate was first observed,
the dip had gradually increased to 60°; it was at this place that pebbles of red
lunestone were obtained from the conglomerate, which contained the following
Ordovician fossils :——Actinoceras tatel, Palearca watttl, Orthis dichotomalis, frag-
ments of trilobites. Underlying this conglomerate is sandstone dipping 61°
south, followed by quartzites and limestones belonging to the Ordovician System,
which gradually increase in dip as they are traced to the north. An examination
of the pebbles, obtained from the conglomerate, reveals the fact that the lowest
strata which of course were deposited first, are almost entirely composed of
fragments derived trom the Ordovician strata, such as sandstones, limestones and
quartzites, while the topmost layers are very largely made up of pebbles derived
from the Pre-Cambrian rocks, These phenomena show that, when the lowest beds
were being deposited the rivers were eroding their valleys out of Ordovician strata, .
but that, when the uppermost beds were being laid down, the erosion had extended
to the underlying Pre-Cambrian rocks. The total thickness of this conglomerate

and conglomeratic sandstone cannot be less than 7000 fect.

62 HORN EXPEDITION—GENERAL GEOLOGY.

V.—Upper Cretaceous.

General Characters.—The supter-structure of the lowest levels around Lake
Eyre has long been known to be argillaceous, and to contain marine fossils, as at
Mount Margaret, Primrose Springs, and Dalhousie. The fauna was at first referred
to the Jurassic period, but has in late years been recognised as contemporaneous with
that of the Rolling Downs series of Queensland. This formation is surmounted
by a hard flinty quartzite or chalcedonised sandstone, varying up to fifty feet in
thickness, which forms the topmost bed of the table-land country, and will be
herein referred to as the Desert Sandstone. Messrs. Jack and Etheridge,
“ Geology of Queensland,” (p. 390), assign the Rolling Downs series to the Lower
Cretaceous epoch; but the facies of the fauna is more akin to that of the
European Upper Cretaceous, while the paleontological differences between it and
the Desert Sandstone are too slight to justify the application of the terms Lower
and Upper to them respectively, therefore we substitute Upper Cretaceous and
Supra-Cretaceous in their place.

Artesian bores around the south and west sides of Lake Eyre have proved
the Upper Cretaceous to be essentially argillaceous. By the courtesy of the
Conservator of Water, we have had the privilege of inspecting the bore material
from the Oodnadatta bore and publishing whatever may be desirable relating
thereto; the boring was near completion on our return to that place. The site of
the bore is approximately at the same level as the railway station, namely, 397
feet above the sea; the bore was discontinued at a depth of 1571 feet, where a
good supply of water was tapped. The whole thickness is essentially argillaceous,
varying from clay, shale, to marly clay, intercalated with which are thin
argillaceous limestones and some sand-beds ; these latter occur at various horizons,
and the chief supply of water was obtained in the basal sands of the section. Thus
the general character of the strata passed through is like that of other bore
sections in the Lake Eyre basin. The deeper seated shales and limestones are
sparingly fossiliferous, and at Oodnadatta the only fossil-record is at 1070 feet in
depth ; whilst a fairly rich fauna has been collected from the outcrop of the top-
most limestone at the various localities previously named. Up to the present no
distinctive rock-formation or fossil-zone has been recognised by which it would be
possible to correlate one bore section with another, and so to arrive at some know-
ledge of the physical structure of the basin and the probable source of its artesian

waters.

The Oodnadatta bore-section is continued above the surface in the low bluffs

to the northward of that township by a limited thickness of argillaceous strata,

HORN EXPEDITION

GENERAL GEOLOGY. 63

sometimes highly indurated, as at Storm Creek, surmounted by the Desert
Sandstone. The prevailing argillaceous formation in the southern area of the
Cretaceous basin continues north to Dalhousie Springs, where fossils oceur, as
described by East* (vu). To Mr. Byrne, in charge of the telegraph oftice
at Charlotte Waters, the writers owe the possession of examples of Criocerias
australis and a coral, preserved in chalcedony, collected in’ the neighbour-
hood of Charlotte Waters; but Mr. East obtained specimens of Lingwla
subovalis in a glauconitic clay-stone at Mount Daniel, which is about twenty miles
north of Charlotte Waters, and the most northern occurrence of a marine fossil of

Upper Cretaceous age within the Lake Eyre basin.

Mount Daniel is 1330 feet above sea level, and its geological structure in
descending order is as follows :—Desert sandstone, 18 feet ; purple and grey shale,
2? feet ; red shale, 40 feet ; yellow and grey shale, thickness unknown. <As we
go north from Mount Daniel, and towards the Upper Cretaceous shore-line, the
shales and clays appear to be replaced by sandstone, which is only what might be
expected, namely, that the rounded sand grains would be deposited nearer the
shore, whilst the lamelle of clay were carried towards what is now the centre of
the basin. In illustration of this change in sedimentation the following sections

are introduced :—

fill, two miles from Goyder River.—(1), Highly ferruginous grit, 15 feet ;
(2), ferruginous sandstone, 65 feet; (3), white friable sandstone, 20 feet ; (4),
ferruginous grit, sandstone and cherty shales, 20 feet ; (5), red iron-stained sand-
stone, micaceous, and in places gritty, 60 feet; (6), friable white micaceous
sandstone containing a moderate quantity of salt, which effloresces out of it,
20 feet; total thickness, 200 feet.

F1ill, between Goyder River and Lilla Creek.—(1), Ironstone, sandstone and
shale cemented by iron, 10 feet; (2), argillaceous sandstone, 1 foot ; (3), ferru-
ginous sandstone, 30 feet ; (4), coarse grit, 3 feet; (5), white friable sandstone,
100 feet ; total thickness, 144 feet.

Mount Musgrave.—(1), Desert sandstone, 10 feet; (2), white friable sand-
stone in beds, which show a slight northerly dip, about 200 feet ; (3), ferruginous,
very micaceous, clayey sandstone, with thin bands of white sandstone, about

200 feet.

* The following species from this locality have been under observation :—Natica variabilis, Maccoyella
reflecta, Modiola inflata, Carditm, sp.

64 HORN EXPEDITION—GENERAL GEOLOGY.

Johnston's Range.—(1), Desert sandstone, 6 to 8 feet; (2), soft white
felspathic sandstone, 25 feet ; (3), more indurated red sandstone, 25 feet; (4),
soft grey argillaceous sandstone, 70 feet. The dip of the beds is about 6° nearly
due south. Giles describes the north escarpment of this line of elevation
as exhibiting successive planes of water-erosion, but his ‘“ water lines” are
simply the effect of alternating bands of variously-coloured rocks, seemingly
horizontally bedded, as viewed on the line of strike (east and west, which is also

the bearing of the escarpment).

The main mass of the Upper Cretaceous reaches as far north as the latitude of
Engoordina, as at Mount Squires, near there, and Johnston’s Range, further west.
North of this latitude much of the country is buried beneath sandhills and river
drift. Bluffs along the margin of the River Hugh, below Alice Well, and to its
junction with the Finke, are composed of unaltered sandstone, and they occasion-
ally occur northward to about seven miles south of Mount Burrell. Of these
outliers Chambers’ Pillar is the most conspicuous. In an amphitheatre-like
depression in the Ordovician limestones, through which flows Alice Creek, there
occurs a micaceous shale as brought to light by a well sinking, which is probably
of Upper Cretaceous age, and if so, then the most northerly occurrence in this part
of Australia. For the most part, the stratification of the Upper Cretaceous is
apparently horizontal, though slight undulations of far-reaching extension prevail
in the northern area occupied by these rocks.

Relation to Artesian Waters.—It has generally been held that the source of
supply of the Natural Artesian Wells on the west side of Lake Eyre was derived
from tropical rains in Queensland absorbed by Cretaceous outcrops, and that the
issue of these waters was along the line of junction of the Cretaceous water-bearing
beds with the Paleozoic rocks on the west margin of Lake Eyre. But the now-
ascertained far-northerly extension of the Cretaceous rocks, and the replacement
of the prevailing argillaceous condition by sandy strata towards the northern
boundary make it probable that the source is, after all, of local origin. Thus, the
Finke River from Henbury to Crown Point flows approximately along the junction
of the Cretaceous arenaceous beds and the impervious Ordovician limestones ; so
also do the Goyder and Lilla Creeks, particularly towards their sources. Moreover
the Cretaceous beds have in the main a slight southerly inclination. It is,
therefore, highly probable that they do absorb some of the flood-waters of those
river-channels, and conduct them to considerable depths in the depressed area
margining Lake Eyre; whilst in no instance do the subterranean waters issue at

the surface at a level so high as that of their conjectural intake. The phenomenon

HORN EXPEDITION—GENERAL GEOLOGY. 65

of extinct mound-springs, as at Dalhousie, may be explained by the circumstance
of a diminished supply, in other words that the level of saturation has fallen below
the level of discharge as a consequence of the desiccation of the climate since

Pliocene times.

ViI.—Desert Sandstone (Supra-Cretaceous).

General Characters.—The greatest thickness presented by this formation, as
observed at Crown Point, was estimated at fifty feet; it consists of three distinct
beds of about equal thickness. The topmost band is a breccia of Desert Sand-
stone fragments cemented by secondary hydrated quartz; the same phenomenon
was noted at Henbury on the Finke River and on the hill-tops about Storm Creek.
The other bands present the prevailing characteristics of the Desert Sandstone,
which is composed of sharp grains of glassy quartz, varying much in size, cemented
by opaque-white highly siliceous matter and more or less stained red by oxide of

iron.

No evidence of unconformability between Upper Cretaceous and Desert
Sandstone was observable between Oodnadatta and the northern contines of the
Cretaceous area, though there is some reason for the opinion the latter overlaps the
former. With one single exception the Desert Sandstone reposes on the Upper
Cretaceous, but at Henbury a few small knolls of Desert Sandstone repose on
Ordovician limestone. The base of the Desert Sandstone is never conglomeratic,
though pebbles of quartz and angular pieces of indurated shale were found at a

depth of ten feet below the summit of Mount Daniel.

Paleontological Features and Correlation.*—Hitherto no fossils have been
recognised in the Desert Sandstone within the area traversed, if we expect obscure
impressions probably of twigs or wood. But the topmost stratum of the table-
topped hills, to the south of Oodnadatta and extending into the basins of Lakes
Torrens and Gairdner, which has the structural peculiarities of the Desert Sand-
stone, except that it is rudely fissile, contains plant-impressions. And in the
south-east part of the Lake Eyre basin extending to Lake Frome a similar flora
occurs in carbonaceous strata, which at the latter locality is associated with marine
fossils of Cretaceous age. A more particular account of these discoveries is now

submitted :—

* The substance of this sub-chapter, under the title of ‘‘ Plant-Bearing Strata in Central Australia,” was read
by one of us before the Royal Society, S.A., 2nd July, 1889, but the publication of it was deferred pending the
result of the bores in the Leigh’s Creek coalfield, which have however no connection with the subject now to he

dealt with,

66 HORN EXPEDITION—GENERAL GEOLOGY.

(1) Area, west of Lakes Eyres and Torrens.

William Springs (123 miles south from Oodnadatta), a well defined impression
of a Cinnamomum leaf on the surface of a characteristic piece of chalcedonised

Desert Sandstone was presented to the 8.A. Museum in 1872.

Bottle Hill and Andamooka (west side of Lake Torrens).—Several slabs of
flaggy quartzites, rich in leaf impressions, were obtained at these localities by Mr.
W. L. R. Gipps in 1876, and presented by him to the University Museum at
Adelaide. Similar specimens from the former locality, collected by Mr. Wentworth
Hardy in 1883, were donated to the same institution.

Lake Gairdner and the Elizabeth River.—In 1883 Mr. Clement Sabine trans-
mitted to the University Museum similar fissile quartzites, showing abundant
plant-remains on their surfaces, from these localities. Accompanying the above
was a block of an excessively fine earthy sandstone, without bedding planes, con-
the casts of the following determinable species of marine bivalves :—JAZaccoyella
barklyt, Cyprina clarke, and Nucula guadrata. ‘The stone was obtained from a
quarry situated at “seven miles 8.W. from Mount Paisley, say long. 135° 45’ and
lat. 30° 15”.”. These facts establish the presence of marine Cretaceous beds and
phytiferous strata in the same area ; and though there is no direct evidence of the
superposition of the latter, yet it may assumed to be so from the circumstance
that a similar, if not identical, quartzite forms the surface-bed over much of the
surrounding country and imparts to the table-topped outliers and low ranges their

characteristic outline.

Arcoona (west of Andamooka).—Similar phytiferous quartzites were presented
by the Government Geologist, Mr. H. Y. L. Brown, in 1888, to the Adelaide
University.

(2) Area south-east of Lake Eyre, de/ween Lake Frome and the Barrier Ranges
In well-sinkings near Lake Frome (a south-eastern extension formerly of Lake
Eyre), sandstones and clays, blackened with coal-smut, were passed through.
From the information and specimens furnished by the Conservator of Water for
the South Australian Government, Professor Tate reported (Trans. Roy. Soc. 8.
Aust., vol. v., p. 98, 1882) that exogenous leaves, all of one species, were abundant
and associated with casts of marine shells; the period assigned was Miocene.
On reconsideration of the evidences in the light of additional and collateral
information, he is of opinion that the marine fossils are of Cretaceous age, as the
known distribution of the marine Eocene is incompatible with its occurrence at this
locality, whilst the Cretaceous age contorms with the area over which undoubted

marine beds are known to cover, The marine fossils indicate the presence of four

HORN EXPEDITION—GENERAL GEOLOGY. 6

—T

genera of bivalves; but as they are represented by casts, specific references are
unreliable. They are Maucula guadrata (?), Aucella sp., Pecten sp.. genus uncertain,
comparable with fig. 16, t. 24, in Jack and Etheridge’s Geol. of Queensland.

The leaves belong to AZagnolia Browntt.

IVyeculuna (on the River Clayton).—Plant-bearing beds have been described by
Mr. H. Y. L. Brown as occurring at this locality. He referred them at first to the
period of deposition of the Leigh Creek coalfield—that is Jurassic, which opinion

* Among the vegetable

has since been amended “to probably of Tertiary age.”
remains collected at this place, I recognise leaf-impressions as belonging to A/nus

Muelleri and Quercus, spp.

The association of Jand-plants and marine fossils is not inconsistent with the
Desert Sandstone age of the Lake Frome beds, as in the extreme north-east of
the vast Cretaceous deposits in Queensland, coaly layers and marine sediments
are interstratified. Hitherto, the only plant-remains descriptively known from
undoubted Desert Sandstone are the ferns Didymosurus? gletchentotdes and
Glossopterts sp.;f neither one nor the other occurs in beds of corresponding age in
Central Australia. Here all the plant species are represented by leaves of
exogens, and of these the following, among many others, are referable to

described species :—

Magnolia Brownii £7¢. Lake Frome.
Cinnamomum sp. William Creek.
Apocynophyllun Mackinlayi, £74. Arcoona.
Bombax Sturtii, £7/ Elizabeth QR.
Eucalyptus Diemenii, £74. Arcoona.
Eucalyptus Mitchell, £77. Elizabeth RR.
Banksia pregrandis, n.sp. Bottle Hill.
Elizabeth R.
Quercus Greyi, £72. Arcoona.
Wyeculuna.
Quercus Wilkinsoni, £7¢. Wyeculuna.
Alnus Muelleri, £77 Wyeculuna.

The flora here indicated is analogous with that at Vegetable Creek and
Dalton, described by Baron von Ettingshausen,? and on paleontologic ground has

been regarded by him as Hocene. The same type of flora is preserved at various
* Parl. Paper, No. 141, 1892, p. 5.
; Jack and Etheridge, Geol. Queensld., pp. 557-559, L802.

¢ ‘Contributions to the Tertiary Flora of Australia.” Mem, Geol. Surv. N.S. Wales, Lss3.
DA

for)
fore)

HORN EXPEDITION—GENERAL GEOLOGY.

localities in Victoria, the age of which is considered by McCoy to be Miocene ;
but it has, however, been shown that the Victorian occurrences are below
marine Eocene, and this accords well with the general fact that wherever the base
of the marine Eocene is reached, lacustrine and plant-bearing beds succeed
in depth. Beds of this age in New Zealand have been called Cretaceo-

Eocene by Hector,

The Vegetable Creek and Dalton beds do not come in contact or in near
location to Cretaceous ; and the marine Tertiaries are absent in New South Wales,

as well as in the country occupied by the Desert Sandstone.

We have, thus, a late Cretaceous deposit and an infra-Kocene one, containing
the same type of vegetation, several species being actually common to the two,
which, if not coeval, must be coterminous; it was because of such considerations
that one of us* had suggested the probability of a paleontological overlap
between Cretaceous and Hocene in Australia.

The fact that the Desert Sandstone of Queensland has not yeielded this type of
vegetation is no argument against the contemporaneity of the phytiferous beds of
Lakes Eyre, Torrens, etc. The same type of vegetation is common to the Laramie-
Cretaceous of North America and the Paleogene of Europe; and the question of
age of the Australian equivalents may be answered in much the same way as was
done in respect of their contemporaries in the northern hemisphere. The Desert
Sandstone of Central Australia by its attachment to the Upper Cretaceous, and
by the occurrence of marine Mollusca of Cretaceous age (at Lake Frome well-
sinkings) must be regarded as coeval with the Desert Sandstone of Queensland,
which, by its intercalated marine sediments is proved to be Cretaceous; though
separated unconformably from the Rolling Downs series (Upper Cretaceous). The
phytiferous beds, which underlie marine Eocene in Victoria and South Australia
and are conformable with them, may conveniently be considered Pre-Eocene.

VII.—Post-Cretaceous Phenomena.

Age of Secondary Silicification.—That the silicification of the Desert Sandstone
was long subsequent to the period of deposition of the original matrix is evident
from the following facts :—

. The uppermost stratum is a breccia, inpregnated and cemented by hydratec
1a t stratu breccia, egnated and cemented by hydrated
silica. Every exhibition of this condition is suggestive of crushing or shattering

of the rock zz situ, without any actual displacement of the fragments.

* Presidential Address, Aust. Assoc. Ady. Science, 1893, p. 35.

HORN EXPEDITION—GENERAL GEOLOGY, 69

2. Denudation of the Upper Cretaceous and Desert Sandstone was consider-
able, both in depth and superticial extent, before silicification supervened. Thus
the marly clays at Dalhousie become porcelainised as they are traced northward ;
and in the neighbourhood of Charlotte Waters a white hard kaolin, which is, how-
ever, not so hard as to resist the knife, is at one spot converted into a porcelain of
a hardness approaching that of quartz. It was from associated beds that Mr.
Byrne obtained silicified casts of Crroceras and a coral. In every example of
silicification of the sediments of Upper Cretaceous age there is no covering bed, and
when the Desert Sandstone is present the alteration is limited to that formation.
It may therefore be inferred that denudation of the Cretaceous plateau preceded
the process of silicification, which, acting from above downwards, atiected whatever
sediment chanced to be at the surface. The texture of the original Desert Sand-
stone permitted doubtlessly greater penetration in depth of the silicifying agent
than was possible in the case of the argillaceous deposits. In the former the
alteration is by infiltration into the interstices of the original coarse-grained sand-
stone, producing a rock which simulates a porphyrite in texture—a clear vitreo-
resinous colloid quartz, compacting sharp quartzose sand-grains. In the latter the

change seems mainly to be that of substitution.

Area Affected by Secondary Silicification.—We have not the data to deliminate
the area over which this chemical alteration has taken place, but that it is vast

may be inferred from the following occurrences :-—

Throughout the Lake Torrens basin and the western section of the Lake Eyre
basin the Desert Sandstone is chalcedonised, extending to the most northern of its
outliers in the vicinity of Henbury. The Ordovician limestones about the sources
of Alice Creek seem also to have been subjected to the same influences, as along
the bedding planes of the somewhat fissile limestones chalcedonic substitution
has taken place for a thickness of an inch or so, An extreme phase of this
structural alteration is the development of noble opal in the Cretaceous rocks at
White Cliffs, about sixty miles in a north-westerly direction from Wilcannia, and
thence passing into South Australia near Cooper Creek. Mr. Anderson* writes
that the chief source of the opal is the Desert Sandstone, in which it occurs in
three following positions :—

Ist. Disseminated in minute fragments throughout the substance of the rock,

2nd. Coating the joints and fractures.

* Records Geol. Sury. N.S.W., vol. iii., p. 30, 1892,

70 HORN EXPEDITION—GENERAL GEOLOGY.

3rd. Occurring irregularly as definitely-shaped pieces, which have resulted

from the replacement of fragments of fossil wood, shells, ete.

Cotemporaneous Phenomena.—The phenomena of silicification of the Cretaceous
deposits is most fully displayed between the Stevenson River and Charlotte
Waters, and here is the metropolis of obsidian bombs and unrolled agates. Bombs
and agates occur widely dispersed over the Cretaceous area in Central Australia,
but we are not aware if any other locality has yielded them in their pristine
condition, the former are most frequently found in an eroded state, and the latter
in a fragmentary condition, and more or less rolled. The agates which abound
between Blood Creek and the River Stevenson, range from the size of one’s fist to
that of one’s head, exhibit a black somewhat scoriaceous exterior and in appearance

resemble those obtained in volcanic scorie.

Origin of the Silicification.—Mr. Kast (viil., p. 52) attributes the change from a
sandy formation to a porcelainised sandstone to immersion in silicated waters,
derive from the decomposition of the metamorphic rocks of the McDonnell
Range, which have wholly evaporated. That the phenomenon of. silicification
implies precipitation from solution cannot be denied, but Mr. East’s view limits
the operation to the final evaporation of the lacustrine waters in which the Desert
Sandstone was deposited; whereas we have endeavoured to prove that considerable
denudation had taken place before silicification could have happened, whilst the
accompanying phenomena, viz., the formation of agates, and obsidian bombs and
Desert Sandstone breccia, seem to demand a common origin. It must be
conceded that the process of silicification has stopped ; that the artesian waters of
the Cretaceous basin do not, and probably never did, possess silicifying properties.
Under the circumstances we hope to be pardoned for speculating upon the origin
of this silicification, which shall, at the same time, be in unison with the require-

ments to satisfy that of the attendant phenomena.

In the first place the occurrence of the obsidian bombs and agates on the
Desert Sandstone plateaus and their slopes could not have been transported there
by water, unless in the form of ice (an hypothesis incompatible with the co-ordinate
features). The origin of the Desert Sandstone breccia was certainly not due to
fracture of the original bed by failure of support arising from denuding action, but
might have been caused by a lava-flow or the deposition of highly heated volcanic
ashes when saturated with water. The obsidian bombs demand volcanic action,
and agates are not infrequently associated with volcanic ejectamenta ; whilst the
silicates of the ash-beds or lava under chemical action would furnish silicated

waters as a source of the chalcedonising action on the underlying rock-surfaces,

HORN EXPEDITION—GENERAL GEOLOGY. fil

The development of agates within the voleanie material was only another phase of
siliceous precipitation. Of this suppositious voleanic formation all that remains
are the agates and the obsidian bombs. The theory seems wild in the extreme
because of the wide-spread silicification, and the absence over its area of any traces
of actual voleanic outbursts ; nevertheless, no other explanation accounting for the

several phenomena appears to us admissible.

VIII.—Tertiary.

Excepting the silt deposits of the present water-ways and the wide-spread
sand-plains, the only Tertiary deposits of any significance are those which indicate
a former water-flow of vaster volumes than at present. These signs are chiefly in
the form of gravels, more or less consolidated, through which the present water-
channels have cut their way, or in the form of terraces margining the valley-plains
through which now flow relatively diminutive creeks. These facts demonstrate
that high pluvial conditions once prevailed ; and, in consequence, perennial flows
in the river-channels of this region were maintained, which, discharging into Lake
Eyre, and supplemented by an Artesian supply in and around it, produced an
inland sea of fresh water, inhabited by alligators (Paddimnarchus pollens) and
turtles, and on its marshy margin dwelt D7frofedon and its fossil associates,
Inferentially the date of formation of these gravels and river-terraces is coeval
with the existence of Diprotedon, whose extinction was due to those physical
causes which destroyed its habitats, and gave Central Australia its present rigor-
ously dry climate. The marsupial lite of this period, on comparison with that
which replaced it, indicates a high antiquity in the number of extinct genera, and
the very high percentage of extinct species, so much so, that the only applicable
time-term is (NEWER) PLIocENk, and not Pleistocene or Post-Tertiary as employed

by some writers.

River Gravets.—The River Goyder, where examined by us, flows between
low cliffs of river detritus, and low mounds extending far back from the existing
channel, are composed of the same material. A section at about two miles east
from the telegraph-crossing comprises from above downwards :—Sandstones some-
what evenly bedded, 5 feet; conglomerate of subangular pebbles of quartzite
and Desert Sandstone, 1 foot; friable white sandstone, current-bedded, with a

coarse sharp grit in the medial part, 20 feet ; total, 26 feet.

The south bank of the Finke River, at Henbury, is composed of gravel
20 feet high.

~I
Lo

HORN EXPEDITION—GENERAL GEOLOGY.

Resting against the escarpment on the north side of Crown Point is a well-
defined shingle-beach, rising to an elevation of, at least, fifty feet above the Finke
Channel; whilst well-rounded pebbles reach up to the base of the Desert Sandstone
on Crown Point, and much gravel is scattered over the low-level country for
several miles northward. East* noted that the channel of the Finke at this place is
strewn with large boulders of red granite, some weighing about a quarter of a ton.

It would appear that prior to the formation of Cunningham Gap (the break
in the escarpment), the waters of the Finke were impounded to form an extensive
lake, during which the shingle collected and reached higher and higher levels as
the lake-water gained depth. The rock-structure of the gorge, as seen in Crown
Point, consists in descending order of Desert Sandstone, about fifty feet, resting
nearly horizontally on false-bedded, friable, felspathic sandstone and purple, hard,
sandy clays. The water-level of the lake reached as high as the base of the
Desert Sandstone, and an easy drainage was presented at its junction with the
underlying beds, which in themselves especially, also because of the southerly dip,
could not offer much resistance to the passage of water. The liberation of the
impounded water was, in the first instance, brought about in all probability by the
undermining of the coping of Desert Sandstone and its final removal. The
irruption of the water was at one stage probably sudden, as a rush of detritus was
piled up in confusion to form the low cliffs bordering the Finke at a distance of

four miles away.

Yellow Cliff, at the south-east bend of the Finke, near Crown Point Head
Station, which is about fifty feet high, consists of :—Yellow and buff sandstone,
strongly false-bedded near the top, intersected by vertical joints filled with
limonite, enclosing pebbles of Desert Sandstone and quartzite ranging from small
gravel to 2} x 4} inches, occasionally two feet cube; the pebbles are somewhat
rounded and smoothed, many of them are standing on edge. At the east end of
this bluff the sandstone is very tumultously-bedded, and in its basal part contains

a conglomerate of about four feet thick.

On the banks of Adminga Creek there is a thickness of thirty feet of con-
solidated river-gravel, consisting of alternating bands of coarse and fine material.
The pebbles, for the most part, consist of Desert Sandstone, ironstone, and

common opal, all of local origin.

River Terraces.—The best exemplification of this feature is in the valley of

Alice Creek near its junction with the River Hugh. Alice Creek is shallow, and

* (viii), p. 44.

HORN EXPEDITION—GENERAL GEOLOGY, 73

about ten yards wide; it meanders through a valley-plain composed of fine silt ;
within about three miles from its junction with the Hugh, the valley-plain is seen
to be bounded on each side by a terrace, at first about half-a-mile apart, finally
converging to less than a quarter of a mile. The terrace is about thirty feet high,

and consists of river-eravels resting, near the base, on white sand-rock.

>

Lacustring Fossin Deposrr.—The extensive development of travertine around
the artesian spring at Dalhousie Head Station, reaching to higher elevations than
the present issue of water, and at one spot containing fossils of a fresh-water
habitus, points to the probability of the former existence of a considerable

lacustrine area. The details of the section are as follows :—

a. l- Co soft.

(a) Fossiliferous rock, exposure about six feet in diameter.

(4) Mound round present springs about ten feet high and 300 feet in diameter.

Water slightly saline and warm. Black peaty soil surrounding mouth.
(c) Débris from (@) travertine deposit.
(2) Compact travertine extending for distance of 300 yards.
(e)

Vifty feet above ¢ Plain red sand loam with loose subangular blocks of

Desert Sandstone (“ gibbers”).

(/) Desert Sandstone rising from eighty to 100 feet above e.

The fossiliferous rock isa gypsiferous tuff, copiously charged with the shells of
Melanta venustula, Brot., AZ. litosa, Gould, AZ. balonnensis, Conrad, Aithinia
australis, Tryon, and Corbicula sublevigata, E. A. Smith. No molluses were found
in the dam conserving the outflow from the artesian spring, and none are existent,
so far as we know, for many miles around. <All the species in the fossiliferous
rock are living. Of these AZelania venustula, Bithinia australts, wand Corbicula
sublevigata were hitherto unknown for South Australia till discovered by the
Expedition. vthinia australis was taken alive in the River Neales and Storm
Creek, near Ooodnadatta ; AZe/ania venustula and Corbicula sublevigata were
found as dead shells in the channel of the Finke at Crown Point. AZe/ania lutosa,
as a recent shell, is known only from Fitzroy Island and Cardwell, N.E. Australia.

10

74 HORN EXPEDITION—GENERAL GEOLOGY,

EXPLANATION OF PLATES.

INDEX TO SIGNS ON THE SECTIONS.

Pre-Cambrian—
a. gneiss,
B. mica-schists.

y- quartzite.
Lruptive Dykes (granite, etc). x.

Ordovician—
a. quartzite.
6. Sandstone.
Dolomite.
. Fossiliferous Limestone.
clay slate.
Micaceous Slates.

. Mudstone with cubes.

S35 SR

Post-Ordovician Conglomerates. 0.
Recent alluvium. VV
(Figures 3, 8, 9 and 10 drawn by R. Tate; Figures 1, 2, 4, 5, 6 and 7 drawn by
J. A. Watt).

Puate I,
Fig. 1.—Section across McDonnell Ranges in the meridian of Ellery Creek.
Vertical scale - - - - 2000 feet to 1 inch.

Horizontal scale - = : 2 miles to 1 inch.

5 2.—Section across South McDonnell Range, near Heavitree Gap.

Vertical scale - - - - 1000 feet to 1 inch.
Horizontal scale - - - 800 yards to 1 inch.
, 3.—Belt Range seen from the south, showing Ordovician sandstone and

quartzite resting unconformably on Pre-Cambrian gneiss and mica-
schist.

» 4.—Section of Ordovician Strata north of George Gill Range.

Horizontal scale — - : = 1 mile to the inch.

Vertical scale - = - 500 feet to the inch,

Horn Expd. Cent. Aust. Geology Plate (.

N)

—_— in fiirts< WS

Bowsens Hole

<V

R.Wendel ith Melb Troedel 6 CO Print

74 HORN EXPEDITION—GENERAL GEOLOGY,

EXPLANATION OF PLATES.

INDEX TO SIGNS ON THE SECTIONS.

Pre-Cambrian—
a. gneiss.
B. mica-schists.

y- quartzite.
Evuptive Dykes (granite, etc). x.

Ordovician—

. quartzite.

. Sandstone.

Dolomite.

. Fossiliferous Limestone.
clay slate.

Micaceous Slates.

te > SP SH SS

. Mudstone with cubes.

Post-Ordovician Conglomerates. 0.

Recent alluvium. VV

(Figures 3, 8, 9 and 10 drawn by R. Tate; Figures 1, 2, 4, 5, 6 and 7 drawn by
J. A. Watt).
Prats I,
Fig. 1.—Section across McDonnell Ranges in the meridian of Ellery Creek.
Vertical scale - = : - 2000 feet to 1 inch.
Horizontal scale - = : 2 miles to 1 inch.
i 2.—Section across South McDonnell Range, near Heavitree Gap.
Vertical scale - : E - 1000 feet to 1 inch.

Horizontal scale - - - 800 yards to 1 inch.

5 3.—Belt Range seen from the south, showing Ordovician sandstone and
quartzite resting unconformably on Pre-Cambrian gneiss and mica-_
schist.

» 4.—Section of Ordovician Strata north of George Gill Range.

Horizontal scale — - - - 1 mile to the inch.
Vertical scale - - - 500 feet to the inch,

Horn xpd. Cent. Aust. Geology Plate |.

\ ‘

North Range
B South Range

ae ry ee
© » alee

a Datum Line 2000ft above Sea Level.
Fig. 3.

( Davenport River

)
AUR Urea

Red Bank Gorge i 5
Datum Line 2000 ft. above Sea Level.

Fig. 5.

2 7

any 8 4 2

lies & = § 5

Sle Krichauff 5 Range Re 4

Elm s 4 2

Missionary Plans | fh SEP ab —_ =
a) > - iS

YEO BET IIE ORE

v
>
c
5
iS 3
i= a
a 2 5 | S
£8 = ¢
James Range se OA 5
akb = aS pk y Ap a 5
FL FIM $ ILLS Ee gE =
RT a cea cy ee is es: > TI of s= fF I oS TON g
DLT TIAL ERAT Sr LAT oe AYE EE TORTS ad
Fig. 7. .

Troedel 2C° Fant

|
}
|
i
}

Horn Exbd. Cent. Aust. Geology Plate 2

»
Bas
G
eo.
a) ED
at n So
Ss : & = re wie N
2 3 sy 5
= g 2% 2
. ca s GR S
Mereenie Bluff N = Pa Ss by
fe ast
5 oS f\«
3 Sa Q
Gi ~ Ss €
= 552
2566" 5 ae
= Se
5

“- < Datum Line 2000 feet above Sea, x x oe e ?

N.10° W. S.10°E.

Hells Gates.

42.3.4 Wall-ltke Masses of Quartzites
Fig. 8

*y y

\

=
= ad ene < : a
al oss foe Horn Valley 3
p 2 ed =
a 2 (PAG s
Ss 9c
s X P20 "j — 8B \
3 2 ee £ Wh fy \ ie AMTAGIEN NN \
Sore. * MMe) Neos WAAAY aS A
ENE LEN Sp a

Distance four Miles

Fig. 9

R Wendel lith, Melb. Troedel & G? Print

HORN EXPEDITION—GENERAL GEOLOGY. 15

Fig. 5, 6 and 7,—Section from the McDonnell Ranges in the north to Levi Range

in the south.

Horizontal scale. - : 2 miles to the inch.
Vertical scale : 2 - 1000 feet to the inch.
- ).——Section across the McDonnell Range to the Missionary Plains.
- 6.—Section across Missionary Plains and the Krichauff Range.
Ps 7.—Section across James Range and Levi Range.
Puate II.
* &.—Section through Ooraminna Pass.
Jlorizontal scale © - = E 3 inches to 4 miles.
Vertical scale - - - } inch to 100 feet.
Pe 9.—Section through Gill’s Pass.
Horizontal distance - : 4 miles.
. 10, -- Section from Mereenie Bluff to Belt Range.

Horizontal distance - = = - 24 miles.

104

ECON OMUEE GEORGY.

Dye An VA I VA Be Se.

A.—GOLD.

The highly metamorphic character of the Pre-Cambrian rocks of the
McDonnell Ranges, their greatly disturbed state, their extensive development,
and lastly the presence of numerous intrusive masses varying much in composition,
are all circumstances favourable to the development of mineral deposits in them.
Gold is the only mineral that has been found in payable quantities in these ranges,
and that only in a very limited area of about fifty square miles, situated seventy
to eighty miles E.N.E. of Alice Springs, on the Arltunga or Paddy’s Hole gold-
field. Although, as just stated, gold in payable quantities has been found on the
above-mentioned goldfield, yet alluvial gold in small quantities has been found also
near Winnecke’s Depot, Bald Hill, and in some of the gullies in the Georgina
Range.

The greater portion of the alluvial gold has been obtained from a red clayey
washdirt occurring in the narrow gullies which take their rise in a low range.
The sinking is exceedingly shallow over the entire field, ranging from a foot or two
up to eight or ten feet, the average being about four to five feet. The bottom is
often very soft, being usually formed by gneiss, which is in a very weathered state,
and therefore soft and friable. The concentration of the gold in the washdirt has
not been satisfactorily accomplished, necessitating in many instances the washing
of the greater part of the alluvium, as the overlying alluvial detritus is often as
rich as the so-called washdirt. Much of the gold won from the gullies is very fine,
a character shared by much of the reef gold also, and consequently difficult to
save. The largest nugget found on the field was taken from Red Gully, and
weighed two ounces three pennyweights. ‘ Surfacing” has been attempted in a
few places, notably on the west side of Kangaroo Creek, where the surface was
removed to a depth of six to eight inches. Owing, however, to the scarcity of
water, and the heavy expense of carting it, when obtainable, to the claims, this

work had to be abandoned as unprofitable, in spite of a fair yield of gold.

The most important auriferous quartz reefs have a prevailing due north

and south trend, and their gold contents show a remarkable uniformity. The

HORN EXPEDITION—-ECONOMIC GEOLOGY.

country-rock includes metamorphic gneisses and mica schists, intruded by eruptive
dykes. Where not absolutely vertical the underlay is almost without exception to
the west, and varies from 5° to 10°. The outcrops of these reefs, which are not,
as a rule, traceable for any great distance, vary in width from four inches to two
feet six inches, while at the bottom of trenches and shatts the width varies from
three inches up to four feet six inches. Taking the average of ten reefs, the width
at the surface was found to be twelve inches, while at an average depth of twenty-
one feet it was fifteen inches. Gold is contained not only in the veinstone but
occasionally and in a less degree in the selvage also, on one or both sides of the
reef. In nearly all the reefs the gold is associated with gossary quartz, some of
the best results being obtained from a spongy siliceous matrix, which crumbles
easily when subjected to pressure. The oxide of iron has been derived from the
oxidation of iron pyrites, and in many cases of copper pyrites also. Derived from
the copper pyrites, or in some cases from sulphides of copper, there are present the

green carbonate (malachite) and the blue carbonate (azurite) of copper,

The following is as complete a list as possible of the results of samples taken

for treatment to the Huntington Mill erected at Claraville :

Name of Mine. Quantity Treated. Yield of Gold per Ton. Remarks.
Monarch - = = ©. Tons - loz 2dwts. - —
Wipe Out - : - 10 ph) cer LORS, - —
Matrix - : - = 1 3 : ess - —
Orient - : 3 - OL ,, 2 Nes eee - —
: : Said not to be picked
Round Hill - - - 4, » Gor a ue
2 | stone
bn P { Probably heavy loss
rm - = : 2) ee = 10dwts. — - i :
5 | during treatinent
Extension of Bee Hive. - a re : iis p —
Wheal Mundi = 2 Boe = thozs < iliac : =
Wheal Fortune 3 roe . - oi tase : a
” i ~ 20 ” - 17 ” =~
Name of mine unknown | , ;
7 ee - LG 5, = ——
to ime : - - j
"2 . 14 = - loz 4. ,, : ==
” ” 10 ” 7 l ” 3 ” is ees
” ” 12 ” = 1 ” 3 ” of —

The total result of these crushings is that 145 tons yielded 1400z. 10dwts., or
at the rate of over 19dwts. per ton.

78 HORN EXPEDITION

ECONOMIC GEOLOGY.

B.—MICA.

On the north side of Hart Range intrusive dykes of a very coarse-grained
granite occur, from a few of which a large quantity of mica has been taken and
despatched to Europe via Adelaide. Only a few of the most promising of these
dykes have had any attention given to them, and on these very little systematic
work has been done. The reason for this is that, owing to the many drawbacks,
among which may be mentioned their enormous distance from a railway and want
of capital, it has been found necessary to pick out the best of the mica obtainable
at or within twenty or thirty feet of the surface. As the descent was being made
from the summit of Hart Range, near Mount Brassey, to the valley on the
north side, bright glistening patches could be seen dotted about, indicating the
position of these granite dykes. This glistening effect was produced by the reflec-
tion of the sun’s rays from the surfaces of innumerable sheets of mica, derived
from the breaking up of the large crystals of this mineral, that were liberated as

the weathering of the granite progressed.

The Oolgarna Claim is situated on the western slope of a short northern spur
of Hart Range, and about 300 feet above the valley. A large granite dyke occurs
there, worked at the time of my visit by Messrs. Hall and Chambers, from which
mica was being obtained at and near the surface. This dyke has intruded the
gneiss almost vertically, with a N.W. and 8.E. strike. Besides the purely surface-
work an open cutting twenty-five yards long has been made on the trend of the

mass, the height of its eastern face being from fifty to sixty feet.

In the cutting the distribution of the constituents of the granite could be
readily perceived. The felspar, of which there are two varieties, is developed on
an exceptionally large scale. Some detached pieces must have weighed from one
to two ewt. Next in size is the quartz, large, clear, glassy masses of which were
seen intimately associated with the felspar, with which it is often intererystallised,

even on a large scale,

The mica, the only mineral commercially important, was found to be largely
developed near the walls of the dyke, and to a less extent towards the centre of
the mass. That occurring on or near the surface, or near the walls, is usually
more or less stained with oxide of iron, and perhaps manganese also; while that
obtained from the parts of the rock out of reach of percolating water, Z.e., towards
the centre of the mass, is clear and without stains, though somewhat dark, and
generally rather smaller in size. Besides this marketable mica (AJZuscovite), there

occur at rare intervals somewhat large masses of a very dark mica (4voéize), the

HORN EXPEDITION—ECONOMIC GEOLOGY. fe)

lamin of which are much bent and opaque, even in thin plates. The largest piece
of Muscovite mica obtained from this claim was, as I was informed, nearly six feet
in length. The mica was cut into rectangular plates varying in size by half inches,
from a few inches up to a foot or more in length, the cutter making the most of
the mica, while no attempt was made to cut it into sizes to suit the market.
When cut it is packed at the mine and conveyed by camel teams to Oodnadatta, a

distance of more than six hundred miles.

During our visit only the mica from the surface, which is, as stated above,
stained brownish-black or reddish-brown by peroxide of iron or manganese, was
being cut and despatched, as there was said to be a good demand for that class of
mica for electrical purposes, the unstained varicties being of course too costly to be

applied to such a use.

On the opposite slope of this spur, and a few hundred feet below its summit,
there is situated a mica claim, the ownership of which was in dispute. The
granite at this claim strikes in an E.S.E. and W.N.W. direction, and has an
underlay of about 45° to the S.S.W. A tunnel from eight to ten feet in height
has been driven into the hill along the course of the dyke for a distance of thirty
feet. The mineralogical composition of this granite is much the same as that of

the Oolgarna granite, with the exception that in the former no biotite was observed.

The muscovite mica, though comparatively free from oxide of iron stains, was
marked with light green spots, which would detract somewhat from its value. The
best of the mica occurs near the south wall, and usually one or more crystal faces
are developed. ‘The largest sheet obtained from this dyke measured, when uncut,
two feet long, two feet wide, and eighteen inches thick ; and, when cut, cighteen

inches in all dimensions.

Six miles west of the Oolgarna claim, and two miles east of Mount Mabhelle,
another granite dyke is situated, which was being worked by Mr. Luce’s party.
The mica was obtained for the most part from shallow open cuttings. A. shaft,
however, has been sunk on the dyke to a depth of twenty-seven feet, at the bottom
of which the dyke was found to have narrowed down from five feet, its width at
the surface to three feet. No mica of any value was obtained from the shaft,
which was put down with the intention of driving eastwards along the trend of the
dyke, to test its mica contents below the point where it appears widest at the
surface. In the case of this dyke, too, the largest mica plates were obtained in
close proximity to the walls. The mineralogical composition is identical with that

of the granite dykes described above. Further west good mica has been obtained

80 HORN EXPEDITION—ECONOMIC GEOLOGY.

from Pope’s and Mount Riddock claims, some of it being of a beautiful ruby tint.
The greater portion, however, of this mica was much spotted. No information
with reference to the financial aspect of this industry was obtainable, owing to the
existence of great rivalry between those interested in the several claims. An
examination of the optical properties of this mica shows that the optic axial plane
lies across the symmetrical track or guide-line of the percussion-figure. This fact
places it in Tschermak’s first order. The angle c:& (axis of greatest elasticity) is
inappreciable, and the angle between the optic axes is large. Thin cleavage flakes
of the dark mica (ézof/ife) which are of a dark brownish-green colour, give a

uniaxial figure, the angle c:& being inappreciable.

The following explanation is suggested of the observed fact of the occurrence
of the greater part of the large mica crystals near the walls of the dyke :—An
examination of the hand specimens makes it perfectly clear that the mica was the
first mineral to commence the process of crystallising out. As that portion of the
granite near the walls, consequent upon the deprivation of some of its heat by
contact with the neighbouring rocks, would be the first to cool sufficiently to allow
crystallisation to proceed ; it is there that we would have the nuclei of the future
crystals formed. The result of this would be the formation of crystals of mica near
the walls ; while, judging by the large dimensions of the crystalline constitutents,
the bulk of the igneous mass was, and for a considerable time remained, liquid.
The mica crystals would, therefore, attract to themselves the necessary molecules,
which would be enabled to answer to the attracting force as long as the mass was

sutliciently fluid.

The mica crystals would not, however, become distributed through the mass,
as they would naturally rapidly avail themselves of the molecules that were in
close proximity to them, and thus become too large to be influenced by the currents
that bring within their sphere of attraction the molecules needed for their growth.
So an undue proportion of the mica substance would crystallise in close proximity
to the walls, leaving the bulk of the rock with less than its due proportion of this

mineral, felspar and quartz greatly predominating towards the centre of the mass.

C.—GARNETS.

The garnets that were asserted to be rubies, for a short time after their
discovery, occur in large quantities in the bed of the Maude and Florence Creeks,
which take their rise on the Southern slope of Hart Range, and more or less plen-

tifully over the surface of the country drained by these creeks. The best stones

HORN EXPEDITION—-ECONOMIC GEOLOGY. 81

were obtained by washing the “dirt” in the bed of the above-mentioned creeks
until the material is reduced sufficiently to permit the rounded water-worn garnets
to be picked out by hand. Although the garnets are exceedingly plentiful, yet
good unfractured and clear stones are comparatively rare. The fine surface sand
of the beds of the creeks was often observed to have a beautiful claret-red tinge,
due to the intermixture of innumerable small fragments of garnet with the sand.
The source of the garnets was found to be a garnetiferous gneiss very rich in this
mineral, a typical specimen of which was gathered from an outcrop on the banks

of the Maude Creek.

An analysis of some specimens of these garnets has been made by Prof. E. H.

Rennie, with the following result* :—

Silica (SiO,) - - - - 38°48 per cent.
Alumina (ALO,) — - - - : 27-06 m1
Ferrous oxide (FeO) - - - 26:28 9
Lime (CaO) : E - : 1:99 ©
Maenesia (MeO) - - - - 4-20 ‘9
Oxide of manganese (MnO) - - 35 5

“ All the iron has been reckoned as protoxide, while some at least of it exists

as peroxide.”

* On some so-called South Australian Rubies, by Prof, E. H. Rennie, D.Se., Trans. and Proc, and Report of

the Roy. Soe. South Australia, vol. xi. (for 1887-8).

P18 WIR ONE GNG NC,

By WV ES MEGA Viel A ee Sn ad | Vie Ne VA TT,
NEA tsa SC.

(Puates 1-4).

Introduction.

The lithological specimens gathered during the Horn Expedition to the
McDonnell Ranges include examples of sedimentary, eruptive, and metamorphic
rocks. The purpose of this paper is to give merely a short description of the
microscopical structure of some of the eruptive and of a few of the most typical of
the metamorphic varieties. The region from which almost all the rocks here
described were gathered includes portions of the McDonnell and Hart ranges.
A general description of some of the granites has already been given in the
chapter dealing with the “ Geology ” of the region ; there will be added here a few

notes only on the felspars.

Although time has not permitted much detailed work on the specimens here
described, there are one or two points to which we should like to draw attention.
One is the beautifully developed, though very minute, micro-pegmatitic structure
in No. 215. The inter-crystallisation of the felspar and quartz is on so fine a scale
that very considerable magnification is needed to recognise it. It was, in fact, ¢
puzzle for some time, until a general similarity to No. 220, where the structure is
more coarsely developed, gave us a clue to its real nature. Under moderate mag-
nifying powers the appearance is that of a number of compacted grains which do
not extinguish under crossed nicols in any position, but are darker in some
positions than in others. Owing to this, and also to the fact that some of the
grains are built up of sections arranged around some central object, generally a

piece of felspar, the different grains are distinguished from one another.

Another point worthy of notice is the evidence that much of the hornblende
in the diorites Nos. 25, 32, 19, has been derived from augite. These secondary
hornblendes are compact and strongly coloured, the tints ranging from greenish-
blue to brown, while the augite grains are comparatively light in colour. It is

questionable whether this can be considered a “ paramorphic ” change, or whether

HORN EXPEDITION—PETROLOGY. 83

the term “uralite ” can be justly used for such material. Typical uralite, of which
Nos. 73, 105, 123, afford examples, is not strongly coloured, and usually retains
the form of the original augite grains ; the planes of symmetry of the hornblendes
and augites being parallel. In the present cases, on the contrary, the hornblendes
do not appear to have any definite morphological relation to the augites, and they
are strongly coloured, and probably contain much more iron than the latter.
These points would seem to indicate a re-crystallisation of the augite material,
together with either a bleaching of the residual augite, or extraneous addition of
iron, or both, rather than the gradual paramorphic change of material from one
crystalline condition to another. Whether the resulting hornblende, in one case

or the other, is fibrous or not is probably unessential.

In calling attention to this point we desire merely to point out that we have
here rocks containing a large proportion of compact, strongly-coloured hornblende,
and that there is strong evidence that much of it has been formed of material

previously crystallised in the form of augite.

Our best thanks are due to Professor T. W. E. David for his kindness in
allowing the sections to be cut in the Geological Laboratory of the Sydney
University, and to Professor Judd, who so kindly placed at our disposal micro-
scopes and a room at South Kensington for the use of the artist engaged in

lithographing the plates.

SEDIMENTARY ROCKS.

Arkose. No. 213. Plate TIT., Fig. 5. Sp. gr. 2°61.

Ayers Rock, a physical feature of great interest, a description of which is
given in the chapter dealing with the ‘Physical Geography,” is entirely made up
of this rock. A short note is given on this rock because it has been so often
called a granite, and, though bearing a somewhat superficial resemblance to a
granite in its macroscopical features, on examination is found to be a rock of
sedimentary origin. It is composed of more or less rounded grains of quartz and
felspar, with a large amount of cementing material, consisting of brown and red
oxides of iron and a little magnetite, probably derived from biotite which has
entirely disappeared. The felspar grains consist of imicrocline, some of them
remaining fairly fresh, whilst others are considerably kaolinised. Some of the
microcline grains show the carlsbad twining in addition to the characteristic

micro-structure.
LA

84 HORN EXPEDITION—PETROLOGY.

FELSPARS.

Plagioclase. No. 147. Plate III., Fig. 2.

This section exhibits what appears to be an inter-growth of felspar and mica.
There are several pieces of mica with well-marked basal cleavage, showing that the
section is cut at right angles to the basal plane. All the pieces of mica are in
optical continuity, as shown by their extinguishing simultaneously. The felspar
is a plagioclase with very low extinction angle. The section was obtained
by grinding down a cleavage flake parallel to the brachypinacoid (010). On
examination ‘under crossed nicols” the felspar and mica are seen to extinguish
practically simultaneously. It seems probable that the several pieces of mica

formed part of a single plate, which lay parallel to the basal plane of the felspar.

Microcline. No. 18a. Plate III., Fig. 4.

This is a section of microcline obtained by grinding down a basal cleavage
flake, and shows in an excellent manner the “cross-hatched” structure. In the
microcline are to been seen strings of a plagioclase, with low extinction angle,
arranged in a roughly parallel manner. The several plagioclase strings are in
perfect optical continuity with each other, and exhibit the albite type of twinning.
They probably occupy the sites of cracks, which have been filled by a secondary
growth of felspar differing in composition and micro-structure from the original

felspar.

Plagioclase. No. 15a. Plate III., Figs. 5 and 6.

This is a plagioclase that is very common in these granites of the Hart
Range. The albite type of twinning is developed in a wonderfully perfect manner,
and the angle of extinction measured from these twinning planes does not exceed
2° or 3°. The sections were obtained by grinding down cleavage flakes parallel to

the basal plane (001).

In Fig. 6 is given a drawing of another basal section, in which masses of
felspar, exhibiting the characteristic microcline structure, are seen to be enclosed
in the plagioclase. Whether these represent original inter-growths, or cavities
subsequently filled with felspar of a different composition to the original, or a
product derived from the alteration of plagioclase iw situ, it is difficult to decide.

The last seems the most probable explanation.

PETROLOGY.

(o's)
or

HORN EXPEDITION

ERUPTIVE ROCKS.
Micro-pegmatite. No. 220. Plate I., Fig. 1, and Plate IV., Fig. 2a.

This is a holo-crystaliine granitic rock composed of felspar, quartz, dark
ferruginous mineral patches, and what may be termed a groundimass of irregular
grains of micro-pegmatitically inter-crystallised quartz and felspar. There are only
a few scattered grains of quartz in addition to that inter-crystallised with the
felspar. There are, however, many crystals of felspar, some of them having
somewhat idiomorphic contours, while all are rendered cloudy from the presence
of decomposition products. In addition there are several irregular dark patches
consisting principally of red oxide of iron, but also to a less extent of magnetite.
These patches occupy the sites of, and have resulted from the decomposition of, a
ferruginous mineral which has left insufficient evidence to enable its species to be
determined, The greater part of the rock is composed of inter-locking micro-
pegmatitic grains, the boundaries of which are not evident, until the rock is
examined “under crossed nicols.” The drawing of the figure (Fig. 1) has been
made in ordinary light, and a few faint lines have been put in to indicate the
boundaries of the micro-peginatitic grains as seen in polarised light. Several of
the grains exhibit an irregularly divergent arrangement of quartz and felspar rays
branching out from a piece of felspar occupying the centre of the grain. The
central piece of felspar is occasionally observed to be in optical continuity with the
felspar of the surrounding micro-pegmatitic mass. This divergent arrangement
corresponds somewhat to the granophyric structure of Rosenbusch. It has been
noticed that in one or two cases the central pieces of felspar exhibit simple
twinning, and that this arrangement is continuous throughout the external micro-

pegmatitic portion of the grain.

In Plate I., Fig. 1, the felspar of the micro-pegmatitic grains is shown by light

shading corresponding to its cloudy appearance under the microscope.

In Plate TV., Fig. 2a, a small grain exhibiting the micro-pegmatitic structure
has been highly magnified and drawn ‘under crossed nicols,” the felspar being
extinguished and the triangular masses representing the quartz. This specimen

formed part of a pebble from the Mount Olga conglomerate.

Micro-pegmatite. No. 215. Plate I, Fig. 2, and Plate IV., Fig. 2d.

gr. 2°71.

Sp.
This rock is apparently a variety of No. 220, but in this case the micro-peg-

matite is developed on a very fine scale, and is to be clearly made out only under

86 HORN EXPEDITION— PETROLOGY.

high magnification. As in the case of No. 220 the rock has a granular structure
which is well-marked ‘“ under crossed nicols.” A few lines have been put in the
drawing (Plate I., Fig. 2), to indicate the outlines of the grains. The quartz and
felspar components of the micro-pegmatitic grains are frequently arranged in
parallel lines presenting the appearance of innumerable fine striations, which is
well seen in Plate IV., Fig. 24, where one of the constituents is extinguished. At
other times they completely inter-ramify, giving a homogeneous appearance, the
complexity of which is recognisable only under considerable magnification. The

mass of the rock is made up of compacted grains of the above nature.

Tn addition to this there are a few small granules of quartz, and a fair number
of kaolinised idiomorphic crystals of felspar. Some of the latter are surrounded

by inicro-pegmatite arranged in irregular radial sectors.

A pale pyroxene is distributed in small grains through the rock as well as a
fair amount of magnetite, and a little red oxide of iron. Much of the magnetite
as well as a pleochroic bluish-green mineral appears to have resulted from the

decomposition of part of the pyroxene.

An important feature of the rock is the presence in most of the micro-pegma-
titic grains of numerous needle-like inclusions, which are aggregated in diverging
groups. These inclusions are very often absent from the centre of the grains,
apparently not having made their appearance till part of the grain had crystallised
out. Under a high power these needle-like inclusions are seen to be composed of
longulites of a pale green colour, which are irregularly aggregated along straight
lines, and appear to have been formed contemporaneously with the micro-pegmatite.
This specimen was also obtained from a pebble occurring in the Mount Olga
conglomerate.

Granulitic pyroxene diorite. No. 25. Plate I, Fig. 3, and Plate IV.,
Fig la-d, and Fig. 5a. Sp. gr. 3:09.

This is a fine grained rock with a sub-conchoidal fracture, not unlike a basalt
in appearance, but rather lighter in colour. Small dark grains are distinguishable
by the naked eye, and colourless particles of about the same size; the former
prove under the microscope to be augite and hornblende crystals, and the latter
porphyritic plagioclase crystals. It is composed of an aggregate of granular
crystals of felspar, hypersthene, augite, and magnetite, which with the exception
of a few of the felspar and augite crystals are of an uniform size. There are,
however, some porphyritic crystals of plagioclase in lathe-shaped sections, and of

a pale green augite,

HORN EXPEDITION—PETROLOGY. 87

The porphyritic felspars have high extinction angles, between labradorite and
anorthite, and contain numerous inclusions of two kinds:—(1) A fine imicro-
scopic dust, Plate I., Fig. 3, and Plate TV., Fig. 14, occupying the centre of each
erystal, the outer shell being usually free from it. This dust appears to be
composed of globulites, some of which consist of magnetite, while others are
transparent ; and, (2) very fine elongated granules of augite, Plate TV., Fig la,
arranged in the centre of the crystal ina layer parallel to 010. | Occasionally
some granules of augite similar to those in the groundmass of the rock are
included. The external boundaries of the crystals are more or less infringed by

granular augite and hypersthene.

The porphyritic augite, Plate I., Fig. 5, is pale green in colour, similar to the
granular crystals, but showing often a fibrous structure parallel to the vertical axis,
somewhat suggestive of diallage. The extinction angle is, however, as large as
42°. The crystals, as a rule, show platy metallic inclusions, Plate IV., Fig. 5a,
lying parallel to 100, similar to those occuring in some diallage, as well as small
granules of inagnetite. These crystals usually exhibit alteration into green
hornblende, Plate IV., Fig. 5a, the uralite (!) so formed being present in consider-
able amount. These secondary hornblendes are compact, and do not exhibit the

usual fibrous structure of uralite.

The granular hypersthene exhibits a somewhat slight pleochroism, brownish-

ink and green being the predominating colours.
S f=) fo}

The granular felspar appears to have been the last mineral to crystallise out,
and occurs in small clear irregular grains, lamellar twinning being occasionally
visible. All the minerals are singularly fresh and clear. The specimen was
obtained from a dyke intruding gneiss on the northern slope of the Hart Range,
and in close proximity to the large coarse-grained granite dyke, on which the

Oolgarna Mica Claim is situated.

Diorite. No. 32. Plate I., Fig. 4.

The greater part of this rock is composed of typical green hornblende, which
is very clear and fresh, and thoroughly allotriomorphic. A certain amount of
comminuted material of a pale greyish-green colour is present. This has a high
index of refraction and strong double refraction, and probably represents the
débris of some augite grains. These patches of powdered augite are almost
invariably surrounded by grains of hornblende, which seem to pass indefinitely

into the powdered material. This is readily observed by the gradual loss of the

88 HORN EXPEDITION

PETROLOGY.

strong pleochrosim of the hornblende. The rest of the rock is composed of clear
granular plagioclase, with apparently high extinction angles. The hornblende fills
in accurately the spaces between the granules of felspar, while a number of small
felspar grains are completely included in some of the hornblende crystals. In the
mass the rock appears to have been subjected to a certain amount of crushing.
This rock occurs as an intrusive dyke in the McDonnell Ranges, near Fish Water

Hole, on Ellery Creek.

Diorite. No. 19. , Plate I, Fig. 5, and Plate IV.,. Figs. 5%, 6a.
Sp. gr. 2°99.

The essential constitutents of this rock are hornblende and plagioclase. The
felspar is clear and fresh, but shows signs of crushing, the twin lamellae being in
places discontinuous and bent (Plate IV., Fig. 6a). Two sets of twinning are
often to be seen, and a series of solution cavities appear frequently to be developed,
the longer axes of which lie parallel to the trace of the plane 010. Occasionally
these cavities have a dendritic form, and are filled with a yellowish ferruginous
material. Compact greenish-brown hornblende is present in considerable quantity
in large, clear and fresh grains with very irregular outlines, being formed
subsequently to the majority of the felspars. Closely associated with these are
numerous grains of a very pale green augite (Plate L, Fig. 5), shown by
stippling, most of which show in places transition into hornblende (Plate TV., Fig.

5b), which is identical in character with the rest of the hornblende.

This suggests the possibility of much of the hornblende having been formed
at the expense of augite. This view is supported by the fact that the augite
grains have suffered considerably in the crush, while the grains of hornblende show
little cracking or dislocation. At present the hornblende is in considerable excess
of the augite, and in fact appears to form about one-half of the whole mass of the
rock. Inclusions of felspar are common in both the grains of augite and horn-
blende. In a portion of one slide a great number of granular zircons lie included
in the hornblendes ; a few of them are present also in the felspars. This rock

occurs at Mount Brassey, in the Hart Range.

Gabbro. Nos. 109 and 90. Plate II., Fig. 3.

Tn thin sections this rock is seen to be a granular aggregate of crystals of
diallage, plagioclase and magnetite, with a small quantity of greenish decompo-

sition products. Although the pyroxene exhibits more or less well-developed

a he -- OULTLhCh Oh Thr

HORN EXPEDITION— PETROLOGY. 89

erystalline boundaries, it must be placed amongst diallages, in virtue of the
development, especially in the neighbourhood of cracks, Plate IT., Fig. 3, of a fibrous
structure parallel to the vertical axis, and the comparatively low extinction angles,
which seldom exceed 31°. On the orthodiagonal section the optical sign is positive.
The felspars have fairly high extinction angles averaging about 26° or 27°, which
indicates a composition near that of bytownite. Magnetite is rather plentiful, and
in the form of large irregular grains. Fine acicular crystals of apatite occur in the
plagioclase, and traverse small grains of secondary quartz. There are present, as
additional secondary minerals, small pieces of a greenish-yellow mica, with strong
absorption, surrounded by a small quantity of a greenish decomposition product
and a little pyrites. Some of the felspars have been replaced by an aggregate
of minute particles of calcite. This rock occurs, between Slip panel Gap and

Ellery Creek, intruding gneiss.

Dolerite. No. 99. Plate IV., Fig. 64. Sp. gr. 3-03.

This rock is very similar to Nos. 195 and 179. It is a coarse-grained rock

consisting of plagioclase, augite, olivine, and magnetite.

The felspar crystals often present the two (abite and pericline) types of
twinning. There is strong evidence of zoning, which is made apparent by the
“shadowy” extinction. The angles of extinction vary from the exterior to the
centre of the crystals, the external portions often having an almost. straight
extinction, while the central portions extinguish at an angle of about 31°. From
this we may conclude that the outer portions of the felspar crystals belong to the

soda end of the soda-lime series, while the central portions belone to the lime end.

The transition from felspar of one composition represented by the high extine-
tion angles to that of a very different composition represented by the low extince-
tion angles is not perfectly progressive. The process of the separating out of
felspar of a gradually changing composition seems to have received a check at a
given stage, when for a certain space of time felspar of a fixed composition seems
to have crystallised out. This was the most stable felspar under the circumstances,
that is, that most able to maintain a fixed composition in spite of the changes
taking place in the magma. The most stable felspar in this case appears to have

been one with an extinction angle between 18° and 28°,
The augite in thin sections is of a pale brownish-yellow colour.
Olivine, Plate IV., Fig. 64, occurs in irregularly-shaped grains which are

much cracked, the cracks being to a great extent filled with fine grains of
12

90 HORN EXPEDITION—PETROLOGY.

magnetite. <A little chlorite, a few flakes of biotite, and a little iron pyrites are
present as accessory minerals. Granular augite occurs in ophitic patches, enclosing
sometimes two or three felspar crystals. The order of crystallisation appears to
have been as follows :—magnetite, felspar, olivine, and augite. The rock occurs

intruding gneiss near the head of Ellery Creek.

Olivine Dolerite. Nos. 195 and 179. Plate II., Fig. 1, and Plate IV.,
Fig. 4. Sp. gr. 3:07.

The felspar of this rock resembles in all respects that described in specimen
No. 99. The augite has its usual characters, the only feature that need be noticed
is its occurrence in large ophitic masses, well shown in Plate IV., Fig. 4. The
olivine, which is present in large quantity, is almost entirely undecomposed ;_ there
are numerous cracks, however, in the crystals, which are filled with fine magnetite
grains. A few grains of hypersthene are present with comparatively feeble
pleochroism, ¢ being green, and 4 pink. This rock occurs between Slip-panel Gap
and Ellery Creek, as a dyke-intruding gneiss.

Fine-grained Dolerite. Nos. 79 and 121. Plate II, Fig. 2. Sp. gr,
No. 79, 2°95; No. 121, 2°97.

The plagioclase crystals are lathe-shaped and have high extinction angles.
The augite is the ordinary brown basaltic variety occurring in fairly uniform
grains, some of which are quite fresh, while others are altered into pseudomorphs
of chlorite, fibrous hornblende, and probably also serpentine. Ophitic structure is
exhibited in parts. This rock intrudes gneiss between Slip-panel Gap and Ellery
Creek.

Dolerite. No. 64. Plate IV., Fig. 3.

This rock, which is much decomposed, consists essentially of plagioclase,
augite and ilmenite. The plagioclase is much decomposed with the production
probably of a moderate amount of saussurite. The augite has crystallised out
early, there being no inclusions of felspar in it. Simple, and perhaps also
multiple, twinning is exhibited by some of the augite crystals. Alteration has
gone on in places, granular epidote, chlorite, and a fibrous hornblende being
developed. The place of magnetite is taken by ilmenite, Plate IV., Fig. 3,
which occurs in the form of irregular flat grains, exhibiting the characteristic

hatched appearance in incident light. A little secondary quartz and a few

HORN EXPEDITION— PETROLOGY. 91

pieces of a dark brown mica are present as alteration products. This rock

occurs intruding gneiss between Slip-panel Gap and Ellery Creek.

Epidote Rock. No. 65. Plate II, Fig. 4. Sp. gr. 3-20.

This rock consists of epidote, hornblende, and a little felspar mostly secondary.
The epidote, which forms more then one-half of the rock, is irregularly granular,
with the usual pleochroism, and is probably due to the alteration of the felspar,
and in some degree of the hornblende. The latter occurs in crystals, which appear
to have suffered considerably during the formation of the epidote. The pleochroism
of hornblende appears bluish-green parallel to ¢, yellowish-green parallel to 4, and
pale yellow pavallel to a. The pleochroism is uncommon, and a reedy fibrous
structure is apparent in most of the sections, Plate IL, Fig. 4. In parts it shows
alteration into flakes of a brownish mica, This rock occurs on the side of dolerite

intrusion between Slip-panel Gap and Ellery Creek.

Amphibolite. No. 16.

This rock is somewhat foliated with a little secondary quartz in veins. It
is almost entirely composed of crystals of hornblende having a remarkable
pleochroism. The extinction is 20° on the clinopinacoid. The pleochroism is £
strong greenish-blue, br olive green, and @ pale yellow. Some sections exhibit a
very finely striated appearance. A certain amount of mica is also present, some of
which is a dark biotite, the greater portion, however, is a bluish-green biotite,
which is practically uniaxial, and has a pleochroism varying from dark green to

yellow. This rock comes from Claraville in the East McDonnell Ranges.

Uralitic amphibolite. Nos. 73, 105, 123. Plate L, Fig. 6. Sp. gr. 3:06,

In the mass it is composed of greyish-green fibrous hornblende, with a certain
amount of a paler green augite scattered through it. In section by far the greater
portion of the rock is seen to be composed of hornblende, the pleochrosim of which
is pale bluish-green, yellowish-green to nearly colourless. The crystals are
irregularly interwoven without definite boundaries, and have a coarsely fibrous to
patchy appearance in polarised light. The most striking feature is the frequent
development of the prismatic cleavage in the hornblende. Amongst the horn-
blende irregular patches of colourless augite grains remain, and there is little doubt
that these are the remains of pyroxenic minerals, which have yielded the horn-
blende by paramorphic change. The hornblende is in fact fairly typical uralite.
This rock comes from Black Knob, near the head of Elery Creek, in the

McDonnell Ranges.
1A

92 HORN EXPEDITION—PETROLOGY.

METAMORPHIC ROCKS.
Gneiss. No. 76. Plate III, Fig. 1.

This rock is somewhat foliated, which is not apparent in the drawing, as the
section was taken parallel to the foliation planes. Biotite is present in flakes
lying parallel to the foliation. The mass of the rock, however, is made up of
irregular interlocking grains of quartz, with some irregular grains of clear felspar,
together with a considerable number of idiomorphic and much decomposed felspars.
A considerable quantity of epidote is distributed through the mass in short
prismatic forms. This rock was obtained near Ellery Creek in the McDonnell

Ranges,

Fine-grained Gneiss. No. 192. Plate IT., Fig. 6.

Foliation is well marked in this rock by means of numerous parallel flakes of
biotite. The mass of the rock is made up of small grains of quartz and clear tri-
clinic felspar, with a certain amount of highly decomposed felspar. A colourless
micaceous mineral is present in small quantities, which is probably sericite. A
few large porphyritic grains of magnetite are scattered through the mass. This
rock occurs on the south side of Mount Conway in the McDonnell Ranges.

Gneiss. No. 48. Sp. gr. 2:76.

This rock contains a considerable quantity of a yellowish epidote. The
general texture is granulitic, with large porphyritic crystals of pink microcline.
The mass of the rock is a granular aggregate of quartz and microcline. This

specimen came from Haast’s Bluff.

Biotite Gneiss. No. 107.

The constituents of this rock are biotite, triclinic felspar and some quartz, the
whole showing strongly-marked foliation, the felspar grains being elongated
parallel with the foliation. A small quantity of a pale rhombic pyroxene is
present, as well as numerous small prisons of apatite. This rock occurs between
Slip-panel Gap and Ellery Creek in the McDonnell Ranges.

Gneiss. No. 206.

Composed of a fine aggregate of quartz and felspar, a considerable amount

of the felspar being converted in places into epidote. Through the mass

HORN EXPEDITION—PETROLOGY. 95

irregular patches of secondary quartz granules are distributed, which seem to have
a somewhat parallel arrangement. Numerous small flakes of biotite are present,
as well as some sinall apatite prisms. The brown biotite is in part connected into
a green variety. This specimen came from the McDonnell Ranges between Slip-

panel Gap and Ellery Creek.

Augen-gneiss. No. 4.

This rock is of a basic character and allied to the diorites in composition,
quartz being practically absent. The “eyes” consist of grains of triclinic felspar
with a little green hornblende, while the foliated groundmass is composed of
crushed fragnients of felspar, dark brown biotite, and a little hornblende. Besides
the above there are numerous pinkish-brown garnets and small grains of apatite
and zircon. This rock was found on the banks of Maude Creck, in the Hart

Range.

Gneiss. No. 23.

The bands of this gneiss are composed of granules of clear felspar and a little
quartz alternating with layers of decomposed and fractured felspar grains. A pale
granular epidote is abundant, and there are a number of thin irregular flakes of a
white mica (sevicite ?), which in places are aggregated into distinct bands. This
rock formed the walls to the quartz reef on the Wheel Fortune Claim, in the

Arltunga goldtields.

Augen-gneiss. No. 249. Plate IL, Fig. 5.

The mass of the rock is made up of closely compacted “eyes,” of fairly uniform
dimensions, and consisting of grains of felspar mostly triclinic with a few grains of
quartz. Surrounding these “eyes” is a very perfect flow-structure formed by
strings of biotite altering into oxides of iron, and separated by layers of com-

minuted quartz dust probably mixed with secondary quartz.

94 HORN EXPEDITION—-PETROLOGY.

EXPLANATION OF PLATES.
Invi II.

Fig. 1.—AMicro-pegmatite. No. 220 x %.* Section drawn in ordinary light
shows a few clear quartz grains, several “cloudy” pieces of felspar, and
two large black patches of hematite and magnetite. The rest of the rock
exhibits the irregular network of quartz and felspar of the micro-

pegmatite grains, the latter constituent being shaded.

» 2—Micropegmatite. No. 215 x %. Drawn in ordinary light. Micro-
pegmatitic structure very fine, scarcely shown at allin this figure. Shaded
portions are more or less decomposed, felspar crystals usually surrounded
by the radiating inclusions. Faint lines have been drawn to indicate the
boundaries of the grains of micro-pegmatite, although these are only to

be made out under ‘crossed nicols.”

oy 3.—Granulitic Pyroxene Diorite. No. 25 x %. Felspars are colourless,
with inclusions. Augite, both porphyritic crystals and small grains
shown by light shading. Small grains of hypersthene shown by a little
deeper shading. Hornblende by deeper shading. Numerous grains of

magnetite shown black.

» 4.—Diorite. No. 32 x *°. Drawn in ordinary light. Felspar clear.
Hornblende shaded. Mass of comminuted augite shown at the bottom

of the section.
» 0.—Diorite. No. 19 x #7. Drawn in ordinary light. Felspar clear.
Augite grains indicated by stippling. Hornblende shaded to indicate

pleochroism,

6.— Uralitic amphibolite. No. 123 x %. Drawn in ordinary light.

”

PuatE IT.
Fig. 1.—Ovivine Dolerite. No. 195 x %. Drawn in ordinary light. Augite
exhibits ophitic structure. Olivine much cracked with magnetite in

filling cracks.

* The numerator of this expression indicates the magnifying power of the eye-piece and objective used in
making the drawing; but as the image produced is reduced in the drawing one-third of its real size, the absolute
degree of magnification of the minerals of the slide, as represented by the drawing, is denoted by the quotient.

Fig.

ss

Fig.

HORN EXPEDITION—PETROLOGY. 95

75

2.—Fine-grained Dolerite. No. 121 x

Augite, plagioclase, and magnetite readily distinguishable. The more

Drawn in ordinary light.

indefinite parts consist of alteration products—chlorite, fibrous hornblende,

and serpentine.

3.—Gabbro. No. 109 x *%, Drawn in ordinary light. Clear pieces
with needle-like inclusions are grains of secondary quartz with apatite.

Felspar is partly decomposed, and diallage shows fibrous structure.

3. Drawn in ordinary light. Shows

4.—EFfpidote Rock. No. 65 x

granular epidote and dark shaded masses of hornblende.

5,—Augen-gneiss. No. 249 x 72. Drawn in ordinary light, and shows

Oo

?

“eyes” of felspar and quartz, and strings of biotite.

6.—Fine-grained Gnetss. No. 192 x %3. | Drawn in ordinary light.
Section at right angles to planes of foliation. Large black mass is a
grain of magnetite. Parallel flakes of biotite shaded dark. Colourless

grains with well-marked outlines are grains of mica (sericite 4).

Puate IIT.

1.—Guerss. No. 76 x 7°. Drawn in ordinary light. Section parallel to
5 y lg I

foliation planes, Numerous grains of epidote.

2.—Plagtoclase. No. 147 x °3. Drawn in ordinary light. Basal cleavage
of mica well-shown. Rest of slide consists of felspar. Extinction of

mica and felspar is parallel to cleavage lines of the former.

3.—Arkose. No. 213 x *%. Drawn in ordinary light. Clear grains are
more or less rounded particles of quartz. Shaded portions represent
microcline grains. Irregular black patches consist of magnetite and
hematite.

4.—Microcline. No. 18a x °°. Drawn “under crossed nicols.” One-
half of microcline is extinguished. Strings of plagioclase show albite
twinning,

5.—Plagioclase. No. 15a x 73. Drawn “under crossed nicols.” One-
half of the plagioclase is extinguished.

6.—Plagtoclase. No. l5a x 4%. Drawn “under crossed nicols.” — Section

of plagioclase with associated mass of microcline.

96

Fig.

”

HORN EXPEDITION—PETROLOGY,

PuaTe LV.

la.—A Lathe-shaped Felspar. No. 25 x 73°. Drawn in ordinary light,
but with some of the twinning planes shown. Linear inclusions of

magnetite and augite grains, also fine microscopic dust.

14.—A Felspar Grain. No. 25 x 73°. Drawn in polarised light to
show arrangement of minute inclusions. Black lines represent

extinguished twin lamelle.

2a.—Specimen No. 220 x 73°. Drawn “under crossed nicols.” A small

>
o

grain to show micro-pegmatitic structure ; felspar is extinguished.

24.—Specimen No. 215 x 73°. Drawn “under crossed nicols.” A highly
magnified grain of micro-pegmatite showing parallel arrangement of
quartz and felspar. One of the constituents is extinguished. A few

inclusions are shown.

3.—Specimen No. 64 x 4%. Drawn in reflected light. Shows charac-
teristic structure of ilmenite. Three sets of dark lines crossing at 60°.

The black patches represent iron pyrites.

4.—Specimen No. 195 x °°. Drawn in ordinary light to show ophitic
structure.

5a.—Specimen No, 25 x 4. Drawn in ordinary light. A porphyritic
crystal of augite with metallic inclusions surrounded by grains of horn-

blende, which pass almost imperceptibly into the augite.

56.—Specimen No. 19 x 4%. Drawn in ordinary light to show passage

of augite into hornblende.

6a.—Specimen No. 19 x 4%. Drawn “under crossed nicols” to show

bending of twin lamellze of plagioclase.

5
3

. Drawn in ordinary light to show irregular

64.—Specimen No, 99 x %

cracking of olivine crystal and infilling of magnetite.

iorn. cil Hixpl f

xped.Petrology Plate IT]

MP Par t} Wes

PALA ON tO.LOG ¥

By RALPH TATE, Professor of Natural History in the University
of Adelaide.

(With Puates 1, 2, 3.)

LARAPINTINE SERIES (ORDOVICIAN).

1. References to Paleontological Literature of the Larapintine Series.

The discovery of Ordovician fossils in Central Australia is solely due to Mr.
F. Thornton, sometime resident at Tenipe Downs, who brought some of them to
the notice first of Mr. H. Y. L. Brown and afterwards of Mr. C. Chewings, on the
occasion of their visits to him in 1890. The first published announcement of this
discovery was, however, made by Mr. Chewings (1) antedating Mr. Brown’s (2)

by a few months.

I.—Tare, R., in Mr. C. Chewings’ “Geological Notes on the Upper Finke
Basin,” Trans. Roy. Soc. 8S. Aust., vol. xiv., p. 255, 1891, recorded the following
genera and species :—Orthoceras aff. tmbricatum (= Actinoceras tatei, Lth. fils),
O. aff, ibex (=O. ibiciforme, n. sp.), Raphistoma, sp. (=R. brownii, Lh. fils),
Orthis flabellum (=O. leviensis, Eh. fils), Strophomena, sp. (= Orthis dichotomatts,
Tate), and Phacops, sp. (= Asaphus illarensis, “7%. j/s). The author was of the

opinion that the fossils indicated an Upper rather than a Lower Silurian facies.

I1.—Erneriper, R., in Mr. Brown’s “Reports on Coal-bearing Area in
neighbourhood of Leigh’s Creek,” Parl. Paper, No. 158, 1891, pp. 9, 10, and 13, 14,
pl. i, figured and described Raphistoma browntt, Orthis leviensis, and Orthoceras,

sp. ind., and believed them to be of Lower Silurian age.

I11.—Erneriver, R., in Mr. Brown’s “ Report on Leigh Creek and Hergott
Springs,” Parl. Paper, No. 23, 1892, p. 8, pl. i, described and figured Asaphus
(Megalaspis") thorntont.

TV.—Howcnin, W., Trans. Roy. Soc. 8. Aust., vol. xvii, p. 355, 1893,
recorded the occurrence of sponge-rods, to which he applied Zittel’s name of

Llyalostelia,

13

98 HORN EXPEDITION

PALZONTOLOGY.

V.—ErueripGE, R., “A Supplement to Parliamentary Papers,” No. 158,
1891, and No. 23, 1892, pp. 1-7, pl. 1, 1893, adds Asaphus illarensis, Orthoceras
gosset, O. tatei, Endoceras warburtoni and Ophileta gilesi.

VI.—Erueriner, R., in “ Annual Report of the Government Geologist,”
Parl. Paper, No. 25, 1894, pp. 23-26, pl. ili., figures and describes a third species
of Asaphus, A. (Megalaspis) howchini, and indicates by figures the occurrence of
three species of univalves belonging to uncertain genera, and one of Cfenodonta,
besides some supplementary information regarding some _previously-described
species.

2. Fossil Localities.

As already stated, anze p. 56, the fossils occur at one definite horizon in
the main mass of the Laparatine series, embracing shelly limestones and the
immediately underlying sandstones and quartzites. The fossiliferous limestones
were observed in Ilpilla Gorge, Middle Valley (from near the junction of the
Walker and Palmer Rivers to Shakes Plain), between Petermann Creek and
Tempe Downs, Petermann Creek, north-east side of Gill’s Range, by camp on
Laurie’s Creek, and about four miles north (north of Tempe Vale). These locali-
ties are on two lines of outcrop of the same beds. Still further north, the same
series occupies the lowest level of Horn Valley from Mereenie Bluff to Finke
Gorge. The quartzites and sandstone subordinate to the fossiliferous limestones
yielded fossils at Middle Valley, Tempe Downs, between Petermann Creek and
Tempe Downs, north of Tempe Vale, and Horn Valley at Finke Gorge. Quartz-
iferous sandstone and limestones of Chandler’s Range are fossiliferous, as also the
quartzites of the Mount Watt outlier. The species of the limestones and of the
quartzites are distinct, with the exception of Orthis dichotomalis and Asaphus

thorntont.
3. Catalogue of the Fossils of the Larapintine Series (Ordovician).

Crass CEPHALOPODA.

Orthoceras gossei, Etheridge, fils.
Ref.—iv., p. 7, pl. 1, figs. 9, 10.

At once distinguished from associated species by the lateral siphuncle and
absence of annulations.

Loc.—In limestone, Tempe Downs and Petermann Creek,

HORN EXPEDITION—PALMHONTOLOGY. 99

Orthoceras ibiciforme, sp. nov. (Plate I, Figs. 7a, 74.)

Sp. char.—Shell elongate, straight, rate of increase one in seven; section
roundly oblong ; surface ornamented with rounded annulations having an obliquity
of about 8°. The distance from one annulation to another is one-third the major
diameter (in the single example with a test no secondary ornamentation is visible,
but as the exterior is somewhat weathered, the presence or absence of sculpture is
uncertain). Septa 1-5 mm. apart, where the shell has a major diameter of 15 mim.
Siphuncle lateral, but cannot be further described, as in the only specimen contain-
ing septa the two septa only visible are broken down around the siphuncle.

Body-chamber unknown.

Obs.—This species resembles O. c6ex, Sowerby, but the annulations are wider
apart, as four to three. The cross-section of O. zlex seems not to be definitely
ascertained, as Blake “ Brit. Foss. Ceph,” p. 95, says, “it may therefore be naturally
elliptical ;” whilst Foord ‘ Cat. Foss. Ceph., Brit. Mus.,” 1, p. 51, on the other hand

writes “section circular ;” in which latter case the Larapintine fossil is further
distinguished by its elliptical section. Orthoceras, sp. ind., t. 4, f. 5 in Johnston’s

Geol. Tasmania, may possibly belong here.

Loc.-—In limestone, Middle Valley at Tempe Downs, Petermann Creek.

Orthoceras microlineatum, sp. nov. (Plate IT., Figs. 10a, 10d.)

Sp. char.—Shell elongate, straight, rate of increase one in six; section
almost circular, Surface ornamented with slightly elevated, oblique and bisinuate
annulations (seven in a length of 17 mm.); sculptured all over with wavy
threadlets (invisible to the unaided eye), separated by incised lines (about forty in
a width of 5 mm.), which are coincident with the annulations. Siphuncle marginal,
large, nearly one-third the diameter of the shell. Septa and body-chamber

unknown.

Obs.—This Larapintine fossil is much like O. dufonti, Barrande, having the
same general character of primary and secondary ornament, the excentric
siphuncle, and circular section of that species; but the annulations are wider
apart, as fourteen to eight, and the microscopic ornament is very much finer and
densely crowded. Externally it is distinguishable from O. @ictforme by its
circular section and more approximate annulations ; in O. ¢iei/orme there are four
(nearly) rings in a length of 17 mm., whilst there are seven in O. mmcrolineatum in

the same length of shell of equal size.
13A

100 HORN EXPEDITION—PALEONTOLOGY.

Loc.—In limestone, north of Tempe Vale, Laurie’s Creek, Middle Valley at
Tempe Downs.

Orthoceras larapintense, sp. nov. (Plate I., Fig. 3.)

Sp. char.—Shell elongate, straight; rate of increase one in ten; section
circular. Septa rather deeply concave, sutures slightly bisinuate; the distance
between the sutures is about one-tenth the diameter. Siphuncle central, about
2mm. in diameter. The species is founded on a single specimen, which shows
three septal chambers in a length of 8 mm., succeeded by a cylindroid body-
chamber 78 mm. long, and 20 mm. and 28 mm. diameters at the proximal and
distal ends respectively. The subtending apical angle indicates a shell of about

nine inches in length.

Obs.—O. larapintense approximates to O. gosset, from the same beds, in its
narrow septal chambers; but in that species the siphuncle is lateral in position. » -
It resembles also O. ferversum, Blake, in its narrow septal chambers ; but that ~
species has an unsymmetrically placed siphuncle, an elliptic section, and the shell Ss.)
does not taper so rapidly.

Loc.—In limestone, Tempe Downs. \

X 3
Orthoceras chewingsi, sp. nov. (Plate I., Fig. 1.) Yay
f
Sp. char.—Shell elongate, straight, rate of increase one in nine, section oe
circular. Septa distant about one-third the diameter, moderately concave, sutures
direct. Siphuncle central, about 1:5 mm., where the shell has a diameter of
12 mm. Test and body-chamber unknown. This species is based upon two
specimens, the larger of which is a fragment 80 mm. long and 27 mm. diameter at > .
the distal end; it is without septa and siphuncle, though the sutural lines (ten in .
1

number) are distinct. The other specimen is nearly complete, except the body-
chamber, and measures 80 mm. long ; the septa and siphuncle are present. The
two specimens I regard as conspecific, because the rate of increase of the shell and

the sutural distances are the same.

Obs.—This species agrees with O. kinnekullense, Foord, ‘Cat. Foss. Ceph., |
Brit. Mus.,” p. 2, fig. 1, of the Swedish Ordovician in its circular section and
sutural distances, being about the widest known, but it differs from it by its
central siphuncle. Orthoceras, sp. ind., t. 4., f. 9, in Johnston’s Geol. Tasm., may
possibly belong here.

Loc.—In limestone, Laurie’s Creek, Petermann Creek, and Tempe Downs.

HORN EXPEDITION—PALHONTOLOGY. 101

Orthoceras, sp. Etheridge, fils.
Ref.—vi., pl. iii, figs. 13-15.

I have nothing to add to Mr. Etheridge’s description except to observe that
the resemblance to Actinoceras tated is very considerable, though the siphunele is

relatively much smaller and the sutures direct.

Endoceras warburtoni, Eth., fils.
Ref.—iv., p. 7., pl. i., figs. 12, 13, and vi., p. 25, pl. ii, figs. 16-20.

Mr. Etheridge in 1894 (4) figured three siphonal casts presumably of this
species. I now further supplement this interesting discovery by the pourtrayal of
a specimen 77 sztu (Pl. IT., Figs. lla, 114), though from the greater rate of increase
in size of the siphon (one in ten as against one in twenty-three or twenty-four)
probably indicates a distinct species. The stoutest specimen has a diameter of

55 mm., and indicates a rate of increase of about one in eleven.

Loc.—In limestone, near camp on Laurie’s Creek, north of Tempe Vale
’ ’ ’

Petermann Creek.

Endoceras arenarium, sp. nov. (Plate I., Fig. 4.)

Sp. char.—Shell straight, section elliptical (the ratio of the two diameters
about six to seven), rate of increase about one in seven or eight. Siphuncular
cavity included within the septa, marginal, elliptic (the ratio of the two diameters
about eleven to twelve), occupying nearly one-half of the longer diameter of the
shell. Septal chambers varying from 3 to 7 mm, wide at the circumferential
margin, where the longer diameter of the shell is 84 mm. Septa very convex,
broadly imbricating exteriorly, and deeply and abruptly descending at the alveolar
cavity. Test and body-chamber unknown, though the cast of the septal portion of

the shell is smooth.

This species attained to a large size ; a portion has the following dimensions :
Length, 85 mi. ; diameters of the broader end, 84 mm. and 73 mm. ; diameters
of the narrower end, 75 mm. and 69 mm.; diameters of the siphuncle at the
broader end, 33°5 mm. and 18:5 mm. The rate of increase of this and other
examples indicates a distal extension of two feet three inches, but a specimen
collected at Finke Pass (though not preserved) was quite twice as bulky as the
example just quoted. The specimens seem to indicate a distinct species by the

elliptic section of the siphuncular cavity.

102 HORN EXPEDITION—-PALHONTOLOGY.

Loc.—This species is restricted to the quartzites immediately underlying the
fossiliferous limestones at north of Tempe Vale and at Finke Gorge.

Actinoceras tatei, Eth., fils., sp. (Plate I., Figs 2a, 24.)
Orthoceras, sp. ind., Etheridge, fils (ii.), p. 10, t. 1, fig. 4.
Orthoceras tatet, id. (iv.), p. 7.

Obs.—A vertical section of the shell shows that the siphuncle is moderately
swollen between the septa. This structure further separates the species from
Orthoceras saturnt, Barr.. O. elevatum, Hall, and O. excentricum, Sowerby, to
which it bears a certain external resemblance. The position of the siphuncle is,
however, not actually central, as stated by the author of the species. The
largest portion obtained has a maximum diameter of two inches, and indicates a

distal extension of sixteen inches.

Loc.—This shell occurs in great profusion in limestone near camp on Laurie’s
Creek and to the north of Tempe Vale, also at Tempe Downs, Petermann Creek,
Mereenie Bluff, and Chandler Range.

Trochoceras recticostatum, sp. nov. (Plate I., Figs 5a—5c.)

Sp. char.—Shell planorbiform with close (though not embracing) whorls.
Septa simple, with a slight transverse curvature, about 2°5 mm. apart at the
outer circumference of the penultimate whorl. Section of last whorl elliptic ;
siphuncle external. The ornamentation is obliterated by weathering, except on
the back of the last whorl, where it consists of slightly elevated, narrow, straight
cost, separated by shallow interspaces of about one millemetre wide. Test and

body-chamber unknown.

Ods.—From the slow increase of the close whorls this shell may be regarded

as an immature Zyochoceras rather than Gyroceras, though the asymmetry of its
eo

spire is not apparent. It recalls Z. spectosum, Barrande, but the costz are more

numerous and not retrovert on the back.

Loc.—In limestone, near camp on Laurie’s Creek—a unique example.

CLAss GASTROPODA.

Eunema larapinta, sp. nov. (Plate I., Fig. 6.)

Sp. char.—Shell imperforate, pyramidal; whorls three (without apex) of
somewhat rapid increase, usually rather broadly and bluntly but occasionally

HORN EXPEDITION—PALEONTOLOGY. 103

sharply keeled at about the anterior one-third. In the middle line of the posterior
area there is a distinct shallow depression, which, with the revolution of the spire,
decreases in conspicuity, and is finally obliterated on the body-whorl. Surface
apparently without sculpture. Last whorl somewhat flatly depressed below the
bluntly-keeled periphery, thence abruptly sloping to the base. © Aperture rhombic-
oval, about as wide as high; columella arched in the vertical plane, very convex
transversely. Length, 22 mm.; breadth, 16 mm. ; aperture, 12 mm. high, 9 mm,

wide. A large example of two whorls has a length of 34 min.
Loc.—In limestone, at Middle Valley, Tempe Downs.

Ods.—The general aspect of this fossil is that of Aucyc/us, but the columella
does not agree with it or other Littorinidie ; it is rather that of Turbinidee. It
also recalls some of the /leurotomarie, notably the Ordovician Murchisonia
gyrogonta, McCoy, Brit. Pal. Foss., p. 293, pl. i, k, fig. 43, but the keel on the
whorls is not a fascia, and a reference to that genus is not permissable. The

imperforate base removes it from Zyochonema.

Raphistoma brownii, Etheridge, fils.
Ref.—ii., p. 9, pl. i, figs. 1-3.

Obs.—This fossil is abundant in the state of loose casts on the limestone
outcrops near camp on Laurie’s Creek, north of Tempe Vale, and Petermann
Creek. Two specimens show traces of ornament on the underside in the form of
oblique growth-lines and slender undulations, which are abruptly retroverted at
the keel, and thus indicate the presence of a peripheral sinus ; but there is no
trace of a fascial band. A large example has the following measures :— Diameters,
90 mm. and 85 mm. ; height, 26 mm. The diameter of the umbilicus is about
one-third that of the base, but is much lessened with the increasing convexity of

the base.

By comparison of an equally-sized specimen of Raphistoma brownit with the
figure of Straporollus (Macluria) tasmanicus, Johnston, “ Geology of Tasmania,”
pl. v., I am inclined to regard the two as conspecific, but as the base of the
Tasmanian shell is not shown it will not be safe to be positive as to their identity.

A comparison of actual specimens can alone permit of a definite opinion.

Scalites (P) eremos, sp. nov. (Plate ITIL, Figs. 28a, 282.)

Sp. char.—Shell biconic ; spire-whorls four, flat, without sculpture or orna-

ment, separated by a linear impressed suture. 3ody-whorl angulated at the

104 HORN EXPEDITION—PALZONTOLOGY.

periphery, beneath which is a narrow, feebly-impressed band; base convex, imper-
forate, aperture rhombic; columella arched in the vertical plane, very convex
) ’ yi

transversely. Height, 12 mm. ; width, 10°5 mm. ; aperture, 6 x 6 mm.

The weathered test does not permit a correct interpretation of the infra-
peripheral band; but, in association with the trochiform shape of the shell, is

suggestive of Sca/izes rather than Eunema.

Loc.—In limestone, Middle Valley at Tempe Downs, IIpilla Gorge, and at
camp on Laurie’s Creek.

Ophileta gilesi, Etheridge, fils.
Ref.—v., p. 6, t. 1, figs. 6-8.

The species was founded on a small cast. The shell shows that the three
anterior whorls are concave between the keel-like front margin and the suture ;
the spire is hardly elevated above the last whorl, whilst the apical whorls are
sunken ; the ornament consists of linear threadlets, oblique, slightly retroverted at
the keel, five in a width of one mm., probably indicating a labial sinus, and thus
connecting with Raphistoma. Dimensions of two largest specimens :—Diameters,

17 mm. and 13 mm. ; height, 7 mm.; diameters, 19 mm. and 16 mm. ; height, 7 mm.

Loc.—In limestone, camp at Laurie’s Creek and north of Tempe Vale.

Pleurotomaria (?) larapinta, sp. noy. (Plate III, Figs. 29a, 290.)

Sp. char.—Shell depressed conoid, whorls (number ?) subimbricate over the
suture. Last whorl with a flange-like keel, narrowly furrowed at the periphery ;
flatly convex to the suture, narrowly precipitous below the keel, thence flatly
convex to the imperforate base. Aperture subquadrate. The ornament consists
of revolving threadlets, fifteen in a width of four mm. on the upper surface of the
body-whorl, about twenty on the posterior half of the base. Length, incomplete,

12 mm.; width, 13 mm.

Loc.—In limestone, Middle Valley, Tempe Downs.

Imperfectly-known Euomphaloid Shells.

(1.) A common fossil in the Larapintine quartzites at Tempe Downs, north of
Tempe Vale, between Petermann Creek and Tempe Downs, and also at Finke
Gorge, is that indicated by a basal impression, which has been figured by
Etheridge, vi., t. 3, figs. 9, 10.

HORN EXPEDITION— PALEONTOLOGY, 105

(2.) A second species is represented by internal casts and the impression of
the spire; a restoration indicates a shell of the size and general outline of
Luomphalus pentagonalis, wat with a flat inornate spire. It has occurred in sand-
stone at Chandler Range, and in quartzite between Petermann Creek and Tempe

Downs, north side of George Gill Range and at Finke Gorge.

(3.) A third species resembles Ofphileta gilesi on a large scale; but the spire
is more elevated, the upper surface of the whorls flat, and the flange-like keel
imbricates over the suture. Only the impressions of the upper surface in quartzite
were obtained, though common, at Middle Valley (Tempe Downs), and at north of

Tempe Vale.

(4.) A larger shell of the last type is indicated by a similar impression from
twenty miles west of Toko Waterhole in Cairns Range, on the Queensland
border ; it differs in having spiral ridges in addition to the sigmoid growth-tolds of

the last species.
Criass LAMELLIBRANCHIATA.

Genus Isoarca, Minster, 1842.
(Zellinomya, Hall, 1847. Crenodonta, Salter, 1852.)

The distinction of Crexodonta (= Telltvomya) from Lsoarca, which was pro-
pounded by Salter, viz., that the former had simple curved umbones and the
latter subspiral ones, is no longer tenable, as one species of the Larapintine rocks
has the umbones more markedly spiral than any described species of Jsoarca
(sensu stricto), and therefore I adopt Woodward's opinion that Cvenodonta is

synonymic with /soarca.

I cannot formulate any set of characters, based on shape, direction of hinge,
disposition and form of teeth, by which the Mesozoic and Palwozoic species may
be kept in different genera ; indeed, if such a course were followed, it would be
necessary to establish several genera for the Larapintine species alone. The
phrase “ Nucula or Leda-like shells” has not a universal application, as may be
judged from the various species herein illustrated, not one of which resembles
either Mucula or Leda; but associated with the dentition of Zscarxca there is repre-
sented the form of Pectunculus, Arca, Opts, Crassatella, Modtola, ete.; whilst an

extreme divergence to an orbicular outline is presented by Z. orbicu/aris.

Isoarca etheridgei, sp. nov. (Plate IT., Fig. 15).

Ctenodonta, sp., Etheridge, f., vi., p. 24, t. 3, figs. 6-8,

106 HORN EXPEDITION—PALAONTOLOGY.

Sp. char.—Oval-trigonal, inequilateral, umbones anterior and _ directed
forwards ; moderately convex, posterior margin roundly truncated, ventral margin
nearly straight, anterior margin shortly rounded, post-dorsal region depressed.
Hinge-line steeply inclined and straight posteriorly ; less declinous and slightly
curved anteriorly ; teeth numerous, small, regular and transverse, thirty on the
posterior side and ten on the anterior side. Surface of shell marked by strong
folds of growth and coincident striz. Diameters, umbo-ventral, and antero-
posterior, 20 mm.; sectional, 11 mm. Mr. Etheridge’s figures represent a more
oblong shell than my type, and connects with a still more oblong variety, but the
trigonal form is the more common.

Loc.—In limestone, Middle Valley at Tempe Downs, Petermann Creek, by
camp at Laurie’s Creek, north of Tempe Vale, and Chandler Range.

Isoarca eastii, sp. nov. (Plate IT., Figs, 12a, 120).

Sp. char.—Shell transversely oval-oblong, very inequilateral, umbones almost
terminal ; inflated dorsally and medially, somewhat compressed antero-ventrally ;
posterior margin roundly truncated, ventral margin nearly direct but rapidly
curving upwards to the anterior margin ; hinge-line slightly arched and long on
the posterior side, short and almost perpendicular on the anterior side. Hinge-
teeth transverse, arched, regularly disposed, increasing in size from the umbo
outwards, about seven on the anterior side and about fifteen on the posterior side.
Cast smooth, the anterior adductor scar large and deep. Antero-posterior

diameter, 44 mm. ; umbo-ventral diameter, 32 mm.

Var. modioleeformis (Pl. I1., fig. 122) differs by its obliquely cylindrical
shape and more prominent umbos, but is connected with the type by intermediate

gradations. The cast presents a few growth-lines and fine coincident striz.

Loc.—In sandstone and quartzite underlying the fossiliferous limestone at

Middle Valley (Tempe Downs).

Isoarca corrugata, sp. nov. (Plate I., Fig. 8.)

Sp. char.—Shell small, transversely oval-oblong, inequilateral, moderately
convex ; umbones ante-median, incurved, approximate. Anterior side short and
rounded ; ventral margin slightly ecurved medially ; posterior side about twice as
long as the anterior one, slightly narrowing towards the subtruncate margin ; post
dorsal margin straight declinous, antero-dorsal margin slightly concave. Hinge

line with direct, transverse, uninterrupted, close teeth, with narrower interstitial

HORN EXPEDITION—PALHONTOLOGY. 107
sockets, about fifteen on the posterior side and six on the anterior side (but the
actual number may probably be ten ; the hinge-line on the anterior side is incom-
plete in the only specimen showing this part of the interior). Surface ornamented
with about eight strong corrugations and nearly a direct post-umbonal ridge.

Antero-posterior diameter, 6 mm. ; umbo-ventral diameter, 4 mm.

Loc.—Thickly covering the limestone surfaces at Middle Valley (Tempe
Downs), also Ipilla Gorge.

Isoarca orbicularis, sp. nov. (Plate IT., Figs. 18a-é.)

Sp. char.—Shell orbicular, moderately convex, without ornament; umbo
subspiral, large, depressed, obtuse, far-distant from the dorsal margin, almost
subcentral ; the anterior dorsal margin is arched upwards to become adnate with
anterior part of the hinge-area, thus simulating ZHwogyra or the operculum-like
valve of a Reguéenta. Hinge-teeth occupying a semi-elliptic curve, coincident with
the post-dorsal margin of the shell, but receding more and more from the antero-
dorsal margin of the shell towards its anterior extremity. Teeth numerous and
closely-set ; on the extreme posterior side they are curved, thence becoming more
and more directly transverse and smaller, and finally almost obsolete on reaching
the anterior adductor scar. Adductor scars inconspicuous. | Antero-posterior

diameter, 23 min. ; transverse diameter, 20 min.

Loc.—Abundant in quartzite at Mount Watt.

lsoarca crassatelleeformis, sp. nov. (Plate IL, Fig. 19.)

Sp. char.—Shell transversely suboval or subtrapezoidal, subinequilateral ;
anterior side rounded ; ventral margin nearly straight, with a moderately deep
Insinuation post medially ; posterior margin obliquely truncated, the dorsal margin
about equally sloping on each side. Umbones moderately inflated, submedian (a
little anterior) ; posterior area defined by a subcarination extending from the umbo
to the post-ventral margin. Hinge-line with numerous small, transverse teeth.
The surface of the shell, anterior to the posterior carination, is ornamented by
wide, convex folds (about twelve) separated by linear sulci coincident with the
anterior and ventral margins. Inner margin of valves edentulous. —Antero-
posterior diameter, 18 mm. ; wmbo-ventral diameter, 12 mm.; greatest sectional
diameter, 9 mm.

Loc.—Numnerous in quartzite with Z. ordicudarts at Mount Watt.
4A

108 HORN EXPEDITION—PALEONTOLOGY.

Oés.—This fossil presents a remarkable analogy to Crassatella sulcata of the

Eocene of Paris and Barton.

Isoarca opiformis, sp. nov. (Plate IIL., Figs. 16a, 162.)

Sp. char.—Cast quadrate, with a very large, strongly curved, sub-central
approximate beak; the steep posterior slope is demarked by an elevated keel
extending from the umbo to the post-ventral margin ; the anterior side depressed
and projects forwards ; its margin is rounded. Hinge-line arched ; teeth transverse
and direct, about six on the anterior side, about twenty smaller ones on the
posterior side. The test must have been very thick, at least anteriorly, judging
from the large conical cast of the anterior adductor impression. Diameters :—

Antero-posterior, 20 mm. ; umbo-ventral, 18 mm. ; sectional, 18 mm.
Loc.—In quartzite, between Petermann Creek and Tempe Downs.

The only important variation in shape exhibited by this species is in the width
of the posterior area; when at its shortest the umbonal keel hides it when viewed
from above. An extreme form has that area wider, therefore not so steep and
so concealed from view by the umbonal carination. The species name is in allusion

to the external resemblance this fossil has to some species of Ofis, ¢.g., Junulatus.

Isoarca wattii, sp. nov. (Plate II., Figs. 17a, 174.)

Sp. char.—Cast oval-oblong to cuneiform, with very large, strongly curved,
sub-marginal, approximate umbones, rounded in front and attenuated behind ;
ventral margin straight, post-dorsal margin arched. The post-dorsal area is
declinous, arising from the umbonal ventricosity extending to the post-ventral
angle, so much so that the hinge-line is posteriorly hidden when the cast- is
viewed from above. Teeth as in /. ofiformis, few and large anteriorly, numerous
and smaller posteriorly. Diameters :—Antero-posterior, 25 mm. ; umbo-ventral,
16 mm. ; a large example, 32 mm. by 20 mm.

Loc.—In quartzite between Petermann Creek and Tempe Downs, associated
with J. ofiformis, from which it differs by its cuneiform shape.

Palzsarca wattii, sp. nov. (Plate IT., Fig. 14.)

Sp. char.—Shell transversely oblong to obliquely rhomboid, moderately ventri-
5 ] ) Me
cose; umbones almost marginal, incurved and approximate; anterior much narrowed;

posterior side much expanded, obliquely truncated. Surface of cast marked by

HORN EXPEDITION— PALEONTOLOGY. 109

fine growth-lines, particularly on the post-dorsal area. Hinge-area narrow, with
three parallel, longitudinal, slightly arched teeth posterior to the umbo ; anterior
teeth two, parallel. Dimensions of figured specimen, which is of small size :—
Antero-posterior diameter, 36 mm.; umbo-ventral diameter, 21 mm.; greatest
dorso-ventral width near to the posterior margin, 27 mm, A very large example

measures 60 x 30 mm.

Loc.—In quartzite and sandstone, Tempe Downs, north of Tempe Vale, and

Finke Gorge.

Obs.—This species has some resemblance to the Ordovician species, P. drd/ings-
tana, Salter, and P. heads, Billings, in its arca-like shape, but is distinguished by
its submarginal umbo and dilated post-dorsal area; but it apparently exactly
resembles AZodiolopsis truncatus, Hall, from beds of corresponding in Ohio and
New York, judging from the figure of that fossil on pl. iL, fig. 13, in Report Geol.
Surv. Ohio, vol. ii., p. 86, 1875.

Palearca tortuosa, sp. nov. (Plate IIL. Fig. 31.)

Sp. char.—Cast triangularly trapezoidal in form, rapidly widening posteriorly ;
axis oblique, corresponding with a high vaulted angulated ridge from the umbo to
the postero-basal angle, on each side of which the slope is precipitous, more so
dorsally than ventrally. Hinge-line straight, umbo at about the anterior one-
sixth; hinge-area of moderate width, marked by two parallel and longitudinal
teeth, which extend for the whole length of the posterior side. Anterior side of
shell somewhat wing-like dorsally ; posterior margin nearly perpendicular to the
hinge-line. Surface of the cast marked by faint folds, which are slightly sigmoid
on the umbonal ridge. Length of hinge-line, 23 min. ; of umbonal ridge, 26 im. ;

of posterior margin, 16 mm.

Loc.—In quartzite, Mount Watt and between Petermann Creek and Tempe

Downs.

Pteronites micans, sp. nov. (Plate I., Fig. 9.)

Sp. char.—Shell transversely elongate, narrow lanceolate ; hinge-line straight ;
beak small, nearly terminal; anterior very short and narrowly triangular ;
posterior side truncate ; surface with six equidistant radial ridges. The cast of
the hinge-line presents a narrow parallel ridge terminating anteriorly at a small
pit, which may be interpreted to indicate a long cartilage furrow posterior to a

cardinal tooth. But for these characters the fossil might have been mistaken for

110 HORN EXPEDITION-—PALHONTOLOGY.

ffyolithes. Total length of hinge-line, 9mm.; umbo, 1°5 mm. from the front ; width

of posterior margin, 3 mm.

Loc.—In limestone, Tempe Downs.

Conocardium, sp. ind. (Plate IL, Fig. 13.)

The fossil here represented is a cast, which by its shape may possibly be

referable to Conocardium.

Loc.—In limestone, Tempe Downs.

Ciass BRACHIOPODA.

Orthis leviensis, Eth., fils.
Ref.—ii., p. 13, t. 1, figs. 5-7 ; v., p. 6, t. 1, figs. 2-5.

Zoc.—In limestone, Ipilla Gorge, Middle Valley, Petermann Creek, Laurie’s

Creek, north of Tempe Vale, Mereenie Bluff, and Horn Valley.

Orthis dichotomalis, sp. nov. (Plate IL, Figs. 20a—d.)

Sp. char.—Shell semicircular, about twice as wide as long, the greatest width
at the long straight hinge-line ; cardinal extremities prolonged into acute, angular,
mucronate wings ; valves concavo-convex. Ventral valve slightly concave, with a
deep depression along the middle, flanked on each side by a slight radial depres-
sion ; umbo sharp, pointed, but not prominent. Dorsal valve moderately convex,
with a median elevation, flanked on each side by a slight radial elevation ; umbo
insignificant and depressed. Hinge-line linear, concave, angular, sculptured with
parallel incised lines. Fissure rhombic, divided medially by the obtrusion of the
cardinal process of the dorsal valve, partially arched over by a pseudo-deltidium

adnate to each umbo.

The ornament consists of slender radial threadlets, increasing in number by
successive dichotomising, about five in a width of 1 mm. at the medial front
margin ; the interspaces are crossed by fine distant growth-lines. Length, 16 mm. ;

width, 30 mm. ; sectional diameter, 3°5> mm. <A very large specimen has length

17 mm., width 35 mm.

Loc.—Abundant in limestone, at Laurie’s Creek, also at Petermann Creek,

north of Tempe Vale, and Mereenie Blutf; in quartzite, north of Tempe Vale.

HORN EXPEDITION—PALMONTOLOGY, A |

Ots.—This species I had originally regarded as a Strophomena, allied to
S. funiculata, McCoy (1.), but despite its Strophomena-like outline and the partial
closure of the foramen, yet by its internal characters it must be referred to Orthis,
among species of which it presents certain analogy to O. a/aza, Sow., and O. phrlipi,
Davidson, differing from both by its crowded radial ornamentation. The concavo-
convex valves separate it from the alate Strophomenze with semicircular outline,

e.g. funiculata, pecten, and applanata.

Crass CRUSTACEA.
Order Trilobita.

Asaphus thorntoni, Eth., fils.
Ref.—iii., p. 8, pl. i1., 1892.

Loc.—In limestone and quartzite, Middle Valley, Tempe Downs.
{ , 1

Asaphus illarensis, Eth., fils. (Plate ITT., Figs. 21a, 214.)
Rep — Ve pe be pl, by, fie, 7,

Perhaps the most important paleontological discovery made by the Expedi-
tion is that of an entire trilobite, as hitherto these fossils had only been known
by pygidia and a few fragments of the thorax. The specimen herein figured
removes any doubt which may have been entertained as to the generic location of

the tail-piece on which Mr. Etheridge established his Asaphus tJarensis.

The facial suture is proper to Asaphus, but in this species proceeds almost
direct from the eye to the front margin. There are seven thoracie segments, but
asthe specimen is broken at the seventh segment and the tail forced back, it is

possible that the eighth segment had become detached.

Head, thorax and tail of about equal length. Glabella clavate. Thorax of
seven (eight?) segments ; the axis as wide as the pleurm, very convex, slightly
tapering, nearly parallel-sided ; pleurze nearly straight, flattened, slightly produced

and bent down at their ends, grooved throughout.

Total length, 62 mm.; greatest width, 40 mm. This species does not seem
to have attained so large a size as some of its congeners ; but a specimen con-
sisting of six thoracic and pygidium has a length of 46 mm., corresponding to a

total length of 80 min.

112 HORN EXPEDITION—PALHONTOLOGY.
Loc.—In limestone, camp at Laurie’s Creek, north of Tempe Vale, Mereenie
Bluff, and Petermann Creek.
Asaphus howchini, Eth., fils.
Ref.—vi., p. 23, t. 3, fig. 1.

A thoracic somite (the axis of which is wider than the pleurz), evidently
belonging to this species, has a total length of 80 mm., thus indicating a size equal

to that of A. ¢ryannus.

Loc.—In limestone, camp at Laurie’s Creek and north of Tempe Vale.

Asaphus lissopeltis, sp. nov. (Plate 3, Figs. 24, 25, 26.)

Sp. char.—Tail rather more than a semicircle, smooth, with a depressed
border. The axis is very distinct, tapers rapidly, and gradually becomes obsolete
just within the depressed border ; the upper one-third is faintly annulated. The
sides in the upper one-third have four faint ribs, the rest of the surface is smooth.

Greatest width, 48 mm. ; axial length, 32 mm.

T figure a glabellum that may belong to this species, which differs from that
of A. tllarensis by the somewhat semicircular track of the facial suture. In asso-
ciation with it is a cheek-piece, which differs by its long attenuated backward

extension.
Loc.—In limestone, camp at Laurie’s Creek and Petermann Creek.

Obs.—This pygidium approaches that of A. 7//arensis in shape, but differs,

inter alia, by the obsolete segmentation.

Hypostomes of Asaphus, spp. (Plate ITT., Figs. 22, 23.)

The hypostome figured and described by Mr. Etheridge, vi., p. 23, t. 3, fig. 2,
has been redrawn (Fig. 23), after freeing the anterior part from its covering matrix ;
it now presents a very different appearance in its anterior margin, which is exces-
sively prolonged and winged. Judging from the matrix, the specimen came from

the limestone on Laurie’s Creek, and in all probability belongs to Asaphus howchint.

Another labrum (Fig. 22) represents a different type; it was obtained at Middle
Valley, Tempe Downs, and may have belonged to Asaphus tlarensis.

HORN EXPEDITION—PALEHONTOLOGY. 1138

Crass EcitnopeRMATA,

The separate joints of slender crinoid stems are not infrequent on the surfaces
of the limestones in Middle Valley, and have also been observed in the same beds
on the north side of George Gill Range. The fragment of stem figured (Fig. 27a)
has a diameter of three mm., and consists of twenty-three joints in a length of

eight mm. An articular face is shown in Fig. 270.

CLASS ZOANTILARIA.

Two species of corals occur in the limestones at Middle Valley and George
Gill Range. One consists of a cylindrical stem with simple forked branches ; the
other forms explanulate thin crusts. They may belong to Che/iles, but the con-
dition of the specimens does not permit of microscopic analysis, and therefore the

generic position is indeterminable.

CLASS SPONGIDA.

The presence of sponge-rootlets in the Larapintine siliceous beds has already

been recorded by Mr. Howehin (iv.). Moreover, the quartzite at Finke Gorge is
y ’ { g

penetrated through a vertical thickness of four inches by cylindrical casts of wbout

1-5 mm. in diameter; and though the casts are larger than //ya/oste/fa rods usually

’ D> Ds - v

are, yet it is more probable that they are so than annelide burrows,

4, Correlation.

By the presence of Lrdoceras and Asaphus, as well as by the aftinities of
many of the Molluscan species, it may safely be concluded that the fauna is
Ordovician ; whilst the remarkable preponderance of /scarce imparts a_ local
feature. Hitherto the only known Ordovician fauna in Continental Australia
is that of the auriferous graptolite slates of Victoria; but that fauna is almost
entirely composed of Graptolites, and is not in any way comparable with that of
the Larapintine rocks. Diligent search was made for Graptolites in the large
development of argillaceous beds towards the base of the Larapintine Series in
Stokes Pass, but without success.

The question naturally arises, are the Larapintine beds and the Victorian
graptolite slates contemporaneous, or, if not, what is their relative position? The
answer is supplied by the sequence of the faunas in the Ordovician System in

Tasmania, 15

114 HORN EXPEDITION—PALHONTOLOGY.

There are recognised two groups of rocks,* (1) The “Auriferous Slate Group”
in the north-east, and (2) “The Gordon River Group.” These two groups do not
come in contact, but from fossil evidence the Gordon Group is considered to
succeed the former. The Auriferous Slate Group contains the remains of
graptolites and a small species of Orthrs, and it may tentatively be regarded as the

equivalent of the Graptolite Slates of Victoria.

The facies of the Molluscan fauna and the lithological characteristics of the
Gordon River Group are in accord with the Larapintine Ordovician, and in marked
contrast with the Victorian type. The absence of Trilobites, which serve to fix the
age of the Larapintine beds, and other salient forms in the Gordon River Group,
may raise a doubt as to their synchronism. As to whether the Gordon River
Group and the Larapintine Series exhibit any closer affinity in their faunas than is
indicated by the generic grouping of their mollusca cannot be ascertained except
by comparison of actual specimens. With few exceptions the fauna of the Gordon
River Group has not been diagnostically made known. Mr. Johnston has, however,
on plates iv., and v., of. cit, figured fourteen species, and attached specific names
to six of them ; but, being undescribed, it is doubtful if any specific identifications
are possible, either from the imperfection of the portraitures or by the omission of
characters necessary to their correct classifactory position. Nevertheless the
resemblances which some of the Larapintine fossils bear to the less indistinct of
Mr, Johnston’s figures lead to the belief that a considerable community in species

will eventually be found to obtain.

The proofs are not conclusive, but there is presumptive evidence that the
Gordon River Group and the Larapintine Series are cotemporaneous and younger
than the Victorian Graptolite Slates. Mr. Johnston, of. c7¢., p. 51, inclines to
regard the Gordon River Group as the equivalents of the Caradoc Series of
England. So do I in respect of the Larapintine Ordovician, not so much because
of its cotemporanity with the Gordon River Group, but rather because of its

representative fauna.

DESCRIPTION OF PLATES.
Puare I.

Fig. 1.—Orthoceras chewingsi, n. sp. Natural size.

" 2.—Actinoceras tate’, Eth., f. a, natural section, showing septa and

siphuncle ; 6, end view of septal surface.

* Johnston, ‘‘ Geol. Tasmania,” pp. 52-63.

A
Fig.

HORN EXPEDITION—PALEONTOLOGY. 115

3.—Orthoceras larapintense, iv. sp. Natural size.

4.—Lndoceras arenarium, n. sp. End view of septal surface.

).—Trochoceras recticostatum, n. sp. a, portion of two whorls, the inner
shewing septa; 4, section of outer whorl; ¢, dorsal aspect of outer

whorl.

6.—Lunema larapinta, vn. sp. Slightly enlarged.

7.—Orthoceras tbictforme, n. sp. a, a cast, natural size; 4, end view of
septal surface of another specimen, with test preserved.

8.—Lsoarca corrugata, n. sp. X 3.

9.—Pleronites micans, 0. sp. xX 3.

PLATe II.

10.—Orthoceras microlineatum, n. sp. a, siphuncular aspect; 4, magnified

portion of test.

11.—£xdoceras, sp. Siphunele, partially embraced by the septa. Siphun-
cular and opposite aspects, s., siphuncle, s/., septal chambers.

12.—Ssvarca eastit, n. sp. a, type, natural size; 4, var. modioleformis,
natural size,

13.—Conocardium, sp. ind.

14.—Palearca waltit, n. sp. Natural size.

15.—Jsoarca etheridget, n. sp.

16.—Js0arca opiformis, n. sp. a-b, casts of two examples.

17.—Js0arca wattii, vu. sp. a, front view of cast ; 4, dorsal aspect of the same.

18.—JLsvarca orbicularis, nu. sp. a, cast slightly enlarged ; 6, wax-impression

of exterior mould.
19.—Lsearca crassatellcformis, n. sp. Wax impression of exterior mould.

20.—Orthis dichotomalis, n. sp. a and 4, dorsal and ventral valves ; c, hinge-

line ; @, section of the closed valves.

Prare IIT.

21.—Asuaphus tllarensis, Eth. t. a and 6, anterior and posterior parts ;
¢, end view.
22.—Hypostome of an Asaphus (A. tllarensis /).

23.—Hypostome ot an Asaphus (dA. howchint ?).

HORN EXPEDITION—PALZONTOLOGY.

. 24.—Pygidium of Asaphus lissopeltis, n. sp.

25.—Glabellum of Asaphus lissopeltis ?

26.—Cheek-piece of Asaphus lissopeltis ?

27.—Crinoid. a, side view of a portion of column enlarged ; 4, articular face
of a joint.

28.—Scalites (?) eremos, n. sp. a and 6, back and front views enlarged.

29.—Pleurotomaria (?) larapinta, n. sp. a and 6, front and back views
enlarged.

30.—Ophileta gilesi, Kth., fil. a, seen from above; 4, oblique view to show

excavated surface of spire-whorls.

31.—FPalearca tortuosa, n. sp.

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'

BOTAN Y.

By RALPH TATE, Professor of Natural History in the University
of Adelaide.

With an Appendix by J. H. Marpen, F.L.S.

CONTENTS.
Cuaprer I.—The Larapintine Flora.

1.—General Physiography and Boundaries of the Larapintine Region.
2.—Botanical Characteristics.
a. Introduction.
6. Salient Botanic Features of the North Eremian Region.
c. The Lowland Vegetation.
d. The Saxatile Vegetation.
3.—Origin of the Flora.
4.—Previous Explorations.
5.—Enuneration of the Flowering Plants and Vascular Cryptogams.

6.—Diagnoses of New Genus and Species.

Cuaprer II.—The Central Eremian Flora.

1.—Physiographic and Botanic Characteristics.
2.—List of Plants new or rare in the Region.

CuapterR I.—The Larapintine Flora,

1. GENERAL PutystoGRAPHY AND BOUNDARIES OF THE LARAPINTINE REGION.

In my arrangement of South Australian Plants, in “A Handbook of the Flora
of Extratropical South Australia,” Adelaide, 1890, I have demarked the area
occupied by the Eremian flora and its subdivisions; therein the northern and
central regions are separated from each other by a latitudinal line through
Charlotte Waters. On physiographic grounds this is a good line, as up to the
tiver Coglin the dominant feature is that of stony table-lands of Cretaceous rocks,

which, though not ceasing there, continue further north, but only as small outliers

118 HORN EXPEDITION—BOTANY.

with extensive intermediate low-level areas covered with loose detritus. Now, as
the result of personal knowledge of the country, I propose to shift the boundary to
the latitude of Engoordina, which will accord better with physiographic and

botanic contrasts.

To the north of this latitude the prevailing feature is a table-land of Ordovician
sandstone of an average elevation of 2500 feet, which rises from a base of about
1000 feet, gradually increasing to the northward to about 2000 or more feet. This
table-land is eroded in long parallel east and west valleys of varying width, from
a few chains to several miles, whilst the river channels break through the inter-
vening tabular ridges here and there to connect one valley with another in deep
narrow precipitous gorges. This is the area which I name Larapintine, from the

native name, ZLavapinta, of the upper and middle Finke River.

On structural and botanical grounds I extend the region to include the
southern watersheds of the Levi and George Gill Ranges, and the northern and
western (Lainages which originate from the western extremity of the Mereenie
Escarpment and its westerly extensions. This region is bounded on the south-east
by remnants of the Cretaceous table-land, and further west by the depressed area
centering in Lake Amadeus ; on the north the Larapintine table-land abuts on and
partially enters into the conformation of the McDonnell Range (sensu stricto, as
deliminated by Stuart), which forms the southern boundary to the elevated plain
called Burt Plain. The route traversed by the main body of the Expedition
practically circumscribed the Larapintine region. To the eastward of the meridian
ot Alice Springs the characteristics of the Larapintine basin are much modified by
more extensive erosion and change in rock-structure, which, in conjunction with

greater aridity, produce a flora much less varied than that of the western section.

2, BoTaANICAL CHARACTERISTICS.

(a) Introduction.—The notions of the generality of people as to the physio-
graphy and geology of this region of Central Australia prove to be vague in the
extreme. What I had gathered from books and personal statements led me to
give such play to my imagination that I had pictured a vast mountain system
capable of preserving some remnants of that pristine flora which existed on this
continent in Paleocene times—probably a beech, possibly an oak, elin, or sycamore.
It was because of such considerations that I drew attention in my Inaugural
Address at the Adelaide meeting of the Australasian Association for the Advance-
ment of Science, 1893, to the desirability of a systematic exploration of the oasis

of the McDonnell Range. The awakening came suddenly and rudely, as there

HORN EXPEDITION—BOTANY. 119

exist no such features as could possibly maintain, under existing conditions, ¢
fauna or flora of a sub-alpine or cold temperature clime ; the region lacks even
those combinations to modify to any extent its species. Nevertheless the region
is not without interest ; indeed one cannot escape the conviction that its exdemic
flora is in a state of decadence, and is being supplanted by an aggressive vegeta-
tion, exotically derived. Moreover, its physiography is unique and on a grand

scale.

Having thus little hope of the discovery of botanical novelties, also because of
extensive botanical explorations previously made, I determined very early on the
journey to concentrate my efforts in the direction of studying the facts and
problems of geographic distribution. The geographic references of many of the
recorded species had to be revised, as such locations as “between the Alberga and
McDonnell Range,” “between Lake Eyre and Alice Springs,” and others, are too
vague to be of special value ; whilst another discordant factor, happily less frequent
of late, is that which attributes the locality of a plant to the place whence the

specimen was transmitted to the recorder.

(6) Salient Botanic Features of the North Eremian Region.—The dominant
feature of the Central Eremian region is the prevalence of salsolaceous plants,
especially over the stony plains and loamy flats ; in the Larapintine region they
are replaced by grasses, and of these a species of 7yzodra (porcupine grass” or,
incorrectly, “spinifex ” of explorers and residents) dominates sandy ground and
the sterile slopes and tops of the sandstone table-lands. The arboreous vegetation
is represented by Casvarina Decaisneana (desert oak), Grevillea striata (silky oak),
Brachychiton Gregoritt, Ficus platypoda, Eucalyptus terminalis, FE. Oldfieldit, Can-
thium latifolium, Livistona Maria, Encephalartos Macdonnelli and others, which
are either restricted to the region or do not pass beyond its southern boundary,
Acacia Farnestana, Atalaya hemiglauca, Eucalyptus tessellarts, and £. gamophylla
are prevalent, though they reach into the northern parts of the Central Eremian
region. Cassia eremophila and Lucalyptus microtheca, which are very characteristic
of the central region, are largely replaced in the northern one by C. phy/lodrnea

and £. ros/rata respectively.

(c) The Lowland Vegetation.—This comprises that of the river-banks, the
loamy plains and sandy ground. It consists, in the greater part, of species widely
diffused throughout the Eremian region, extending far south in South Australia,
eastward into New South Wales and South-west Queensland, and westward to the
shores of mid Western Australia, This portion of the Larapintine flora offers

considerable similarity to that of Shark’s Bay, as enumerated by Baron F. von

120 HORN EXPEDITION—BOTANY.

Mueller (Parl. Report, Perth, 1883); thus, of a total of 332 species, deducting
therefrom ten which are maritime, 187, or 60 per centum, are constituents of the
flora of the Finke Basin; and by very slight extension of that area the actual
number in common is 198. The Orders Zygophyllee, Malvacem, Salsolacez,
Leguminose, Myoporine, and Graminewe, which are most largely represented,
have few species which are not common to the two areas. The Myrtaceze of all
others show the greatest specific distinctness ; thus, of seventeen inhabiting Shark’s
Bay, only three are in common, viz., Hucalyptus terminalis, EF. eudesmoides, and the
ubiquitous 2. rostrata. So also the flora of Nickol Bay exhibits the same affinity,
as, of a total of 185 species listed by Baron F. von Mueller (Parl. Rep., Perth,

1881), 110, or 60 per centum, occur in the Larapintine region.

This type of vegetation constitutes a very large proportion of the whole
Larapintine flora; its species are either immigrants from the Oriental Botanical
Province or are endemic species of extra-Australasian genera. The truly Australian
forms, excepting perhaps among Acacia, Eucalyptus, and a few others, are most
frequently gregarious in isolated colonies, sometimes occupying a few square yards,
or even as much as several square miles. Of the former, Diplofeltis Stuartit,
Catosperma Muelleri, and Ptychosema trifoliolatum may be quoted as examples, and
Brachysema Chambersit and Grevillea eriostachya of the latter. On several
occasions, in the earlier part of our travels, I had passed by an unfamiliar plant,
hoping it would extend as far as our halting-place, near approaching ; but in the
majority of instances the expectation was not realised. Profiting by this
experience, I afterwards let no plant unknown to me go ungathered. It is
because of the sporadic distribution of many of the Australian species that it is

probable that a not inconsiderable number remain to be discovered.

The aggressive nature of the alien plants is exhibited not only by their
extensive distribution, but also by their ability to adapt themselves to extremes of
soil and climate. Such species, among others, as Zribuldus terrestris, Cleome
viscosa, Malvastrum spicatum, Boerhaavia diffusa, Salsola kali, Mollugo hirta, and
Pollichia Zeylanica range from the river-banks and loamy plains to the sandhills,
and surmount the highest elevations of the rocky country. No endemic species
shows such ubiquity, not even Z7iodia pungens, which seenis confined to absolutely
sterile tracts, no matter however great the elevation. Chenopodium rhadino-

stachyum, though not a common plant, has however an equal altitudinal range.

(d) The Saxatile Vegetation.—I cannot write of a mountain flora because the
number of actual species on the table-lands and other high-level tracts is absolutely

few. The exploration of Station Range, of about 500 feet elevation above Tempe

HORN EXPEDITION—RBOTANY. 121

Downs and 2179 feet above sea-level, which forms the south boundary of the

valley of the Walker River at Tempe Downs, yielded nineteen species only ; they

Were -—

Equally poor results attended the ascents of other elevations.

Sida corrugata.

Ficus platypoda.

Dodonvea petiolaris.

Ptilotus incanus.

Acacia aneura.
Thryptomene Maissonneuvii.
Eucalyptus terminalis.
Pomax umbellata.

Aster megalodontus.

Solanum Sturtianum,
Tecoma australis.
Postanthera Willieana.
Eremophila Freelingi.
Callitris robusta.
Andropogon bombycinus.
Anthistiria ciliata.
Avistida calycina.

Eriachne scleranthoides.

Triodia pungens.

Mount Sonder

(4497 feet), the highest elevation explored, yielded rather more species, and the
discovery of two noteworthy plants near its summit was the only recompense for
an otherwise profitless and toilsome day’s work. The same remark will apply to
Mount Gillen, and a list of the species observed during the ascent, most of which
were living near the summit, at not less than about 1000 feet above the base of

its escarpment, here follows :—

Cleome viscosa.
Abutilon otocarpum.
Hibiscus Pinonianus.
Dodoniea petiolaris.
Ptilotus incanus.
Ptilotus Hoodii.
Euxolus Mitchelli.

Chenopodium rhadinostacyhuin.

Boerhaavia diffusa.

Indigofera brevidens-canescens.
Cassia eremophila.

Acacia dictyophleba.
Eucalyptus terminalis.

Eucalyptus gamophylla.

Didiseus Gillenze.
Grevillea agrifolia.

Aster megalodontus.
Pterocaulon Billardieri.
Helichrysum ambiguum.
Helichrysum Kempe.
Goodenia Ramelii.
Solanum petrophilum.
Halgania cyanea,
Pollichia Zeylanica,
Spartothamnus puberulus.
Callitris robusta.
Macrozamia Macdonnelli.

Eviachne scleranthoides.

Triodia pungens.

Tt may be observed that the inclined slopes and summits of all the elevated

masses in the Larapintine region are devoid of soil, the surface presenting the

16

122 HORN EXPEDITION—BOTANY.

appearance of a road newly made with large metal, amongst which porcupine-grass
grows usually so densely that progress is extremely difficult and even painful if the
pedestrian’s legs are not well protected ; though these impediments may be less
discomforting if the tussocks of grass, where not too widely spreading, are availed
of by springing from one to another. The faces of these declivities are channelled
to varying depths from the condition of mere runnels to deep narrow ravines,
which usually terminate in a rock-pool. The majority of the plants occur rooting
in the crevices of the rocky walls bounding these water-ways ; though it is not an
infrequent circumstance to find stately gum trees (Zucalyptus terminalis) and pines

(Callitris robusta) on the scarped fronts of the sandstone table-land.

It is in the gorges of the table-lands and on the basal part of the crage
escarpments and their taluses that a varied flora occurs. These are the habitats
of the chief novelties which impart a peculiarity, almost suz generis, to the Lara-
pintine flora. With few exceptions the species are endemic; thus of seventy
flowering plants, restrictedly rock-dwellers, seven only are of exotic origin, namely,
Capparis spinosa, Hybanthus enneaspermus (but always in the restricted variety
aurantiacus), Trema cannabina, Parietaria debilis, Piumbago Zeylanica, Acyranthes
aspera, and Crotalaria medicaginea. The richer flora prevails on the southern
aspect of the escarpments and on the north walls of the east and west ravines,
and it is very probable that some species remain to be discovered in the many

unexplored rocky recesses of the George Gill, James, and Krichauff Ranges.

The chief arboreous and shrubby vegetation includes //b¢ertia glaberrima,
Sida cryphiopetala, Ficus platypoda, Dodonea lanceolata, D. petiolaris, Mirbelia
oxyclada, Indigofera brevidens, var. canescens, Erythrina vespertilio, Cassia glutinosa,
C. pruinosa, Acacia lycopodifolia, A. strongylophylla, Eucalyptus terminalis,
E. pachyphylla, Grevillea agrifolia, Tecoma australis, Prostanthera Waitkieana,
LEremophila Goodwint, Caltitris robusta and Encephalartos Macdonnelli.

The chief herbaceous plants are Oxalis corniculata, Parietaria debilis, Ptilotus
parvifolius, P. exaltatus, P. Schiwartsii, Crotalaria medicaginea, Aster megalodontus,
A. Ferresi, Helichrysum ambiguum, Isotoma petrea, Scevola ovalifolia, Goodenta
Ramelit, G. Vilmorinie, Ruellia primulacea, Justicia Kempeana, Plectranthus parvt-
florus, Cynoglossum Drummondi, Eriachne scleranthoides, Triodia pungens, and
Cheilanthes tenuifolia.

As already stated, the characteristic vegetation of the Larapintine region is
supplied by its saxatile species. Of these only a limited number extend to far-

reaching localities, eg., Ovxalis, Parietaria, Ptilotus exaltatus, P. parvifolius,

HORN EXPEDITION—BOTANY. 123

Hydrocotyle trachycarpa, Lso/oma petrea, Cynoglossum Drummond, Callttris,
Chetlanthes tenutfolia, C. vellea, and Grammitis rutefolia.

The majority of the Larapintine species was originally discovered within the
region, but in later years this saxatile flora has been known to extend to Mount
Olga, the Musgrave, and Everard Ranges in South Australia, and to cross to the
Cavenagh Range in West Australia. These elevations must therefore be regarded
as botanical outliers of the Larapintine region ; furthermore, the range of others
has been extended north and north-west, far beyond the limits of this remarkable
physiographic area Thus it has come to pass that a few species only remain as

yet restricted to within its boundaries.

3. ORIGIN OF THE FLORA.

In my sketch “On the Influence of Physiographic Changes in the Distribu-
tion of Life in Australia” (Austral. Assoc. Adv. Science, vol. i, pp. 312-325,
1889), I have indicated that the flora of Australia consists of the following

constituent elements :—

1. An immigrant portion derived from at least two separate sources, (a)
Oriental and (4) Andean.

2, An endemic or Australian portion, which is relatively of higher antiquity.

(a). That the Autochthonian constituent, which occupies the south-west

corner of West Australia, was dismembered in Cretaceous times.

(4). That the Euronotian coustituent was superimposed by the Oriental
and Andean incursions. The Andean immigration was probably
coeval with the last glaciation of Australia, which may have been
in late Cretaceous or in Paleocene times, and if so then approxi-
mately cotemporancous with the dismemberment of the primitive
Australian flora, and therefore antedated the Oriental immigration,

which has virtually not ceased since its advent.

(c). That in Post-Phocene times there originated in Central Australia an
Eremian flora developed from Autochthonian and Euronotian
elements, and largely modified by Oriental immigrants and the

species evolved from them.

In the essay above referred to T have dealt with the botanical characteristics
of the Eremian region, and they need not be repeated here, as the main facts

16A

124 HORN EXPEDITION—BOTANY.

relating to the Larapintine flora are embraced therein, Nevertheless some aspects

of the two types of vegetation locally represented may be considered.

The Larapintine flora is composed of :—

I.— Exotic species, chiefly Oriental - - 125
II.—Endemic species of exotic genera — - - 219
I1J.—Endemic species of Australian genera - 270
614

In the appended tables, from which the above summary is derived, Pit/osporum,
Ficus, Cassta, Santalum, and Loranthus are included among the endemic genera for
reasons which are explained at page 131, whilst the alliance with South Africa
through Helipterum, Encephalartos, and others, is disregarded as not affecting the
main issues touching the origin of the Larapintine flora, and they are also included

among the endemic genera.

The species in categories I. and II. belong, as a whole, to the Eremian type
of vegetation, and to these should be added fifty-two in category III., which belong
to genera characteristically Eremian though endemic, though it is possible that
some of them, particularly the vascular cryptogams and aquatic plants may have
formed part of the primitive Australian vegetation. An important factor in the
problem of the origin of a flora, here wanting, is the geological evidence of the
relative periods of introduction of its alien forms, and it is only our knowledge of
the modes of dispersion of plants and the varying rapidity by which unoccupied
tracts may be re-peopled that permit us to infer that the vascular cryptogams are
the first to appear, then the aquatic and paludinal plants, or on coast-lines some
flowering plants by means of water carriage, and lastly the bulk of the terrestial

species.

TabLE oF Exotic GENERA, AND THE NUMBER OF ENDEMIC AND Exotic SPECIES.

Genera Giges pee Genera Sue Bate
Cleome - - Be aie a ets: Ue OL Elatine - - ae gab somal
Capparis - - a 1 Bergia_—- - Sale? 1
Erysimum - - 1 Hypericum - 1
Capsella - - ies Polygala - - - 1
Lepidium - . - 3 1 Zygophyllum — - - 6
Hybanthus - See , 1 Tribulus. - - - 2 1
Drosera - - eae SM CoD ng ge Erodium - - oT

Genera.
Oxalis ; : :
Lavatera -
Malvastrum — - :
Sida :
Abutilon - :
Hibiscus - : :

Gossypium . -

Brachychiton — -
Melhania - =
Waltheria
Corchorus : =
Triumfetta
Euphorbia
Phylanthus

Trema :
Parictaria :
Dodoniea (D. viscosi)
Frankenia : ;
Plumbago : z
Portulaca - -
Claytonia - : :
Spergularia : =
Polycarpiea : =
Gomphrena :
Alternanthera
Achyranthes — - =
Euxolus - : -
Atriplex - :
Chenopodium — - -
Kochia — - ; -
Bassia —- : :
Salicornia : -
Salsola — - - :
Aizoon — - - -
Zaleya - - -
Trianthema -

Mollugo - = :

HORN EXPEDITION—BOTANY.

Endemic
Species.

Exotic
Species.

1

ee

wee

Genera,

Species.
Polygonum - -
Boerhaavia - -
Crotalaria - So
Lotus - - =. J
Psoralea - - - 3
Indigofera - 2
Tephrosia - - 2
ZEschynomene - -
Glycine - - - 2
Erythrina - - Jd
Viena - - - dl
Rhynchosia — - -
Cassia (C. Sophera) -
Neptunia - : -

Acacia (A. Farnesiana)
Tilleea : -
Rotala — - 2 :
Ammannia - -
Lythrum - - -
Myriophyllum - -
Ventilago - -
Hydrocotyle — - -
Daucus - - -
Oldenlandia — - :
Canthium - -
Melothria -
Cucumis. - - -
Aster -
Podocoma - -
Pluchea - : -
Epaltes — - - :
Pterocaulon F -
Helichrysum — - -
Gnaphalium — - -
Siegesbeckia — - -
Wedeha - - -

Bidens — - i -

Endemic

Lo

Exotic
Species,
»

»
a

bw

— pl et

bo

Genera.
Glossogyne
Centipeda
Senecio. -
Wahlenbergia
Erythreea -
Plantago -
Samolus -
Jasminum
Carissame
Cynanchum
Sarcostemma
Demia -
Marsdenia
Tpomea -
Convolvulus
Brewerla -
Evolvulus
Cuscuta -
Solanum -
Datura =
Nicotiana -
Mimulus -
Stemodia -
Limosella -
Buechnera
Tecoma -
Ruellia — -
Justicia -
Plectranthus
Teucrium -
Verbena -
Clerodendron
Cynoglossum
Pollichia -
Heliotropium
Josephinia
Ottelia —-

HORN EXPEDITION—BOTANY.

Endemic
Species.

me =] le ee Oe

en ee ee

HS KH KE bo

Exotic
Species.

1
1

Genera.
Crinum -
Wurmbsea
Typha -
Naias -
Potamogeton
Triglochin
Commelina
Juncus” -
Eriocaulon
Cyperus. -
Heleocharis
Fimbristylis
Scirpus -
Lipocarpha
Fuirena -
Eriochloa
Panicum -
Setaria
Pennisetum
Perotis = -
Tragus
Andropogon
Imperata -
Erianthus
Anthistiria
Aristida -
Stipa 2
Pappophorum
Sporobolus
Eriachne -
Danthonia
Chloris — -
Eleusine -
Diplachne
Triodia = -
Eragrostis

Arundo -

Endemic
Species.

1
l

Lo

Exotic
Species.

OC a nl Sr SO

lo

—

woo— —

HORN EXPEDITION—BOTANY. 127

, Endemic Exotic Endemic Ra
General nder Exot Venere tndemic Exotic
Species. Species. Genera, Species. Species.
Marsilea - : ne: eer 1 Aspidium - - Sk A 1
Psilotum - : - . ia 1 Gramuinitis - a See ]
Adiantum - = 2s we ol Lygodium . Se as fee.” ol
Cheilanthes — - - , eae 2

TABLE OF AUSTRALASIAN GENERA, OR ESSENTIALLY SO, WITH NUMBER OF SPECIES
TO EACH.

Genera. Spee: Genera. eal
Hibbertia - - : 2.3% Tsotropis - : : : - 9
Stenopetalum - : z = 3 Mirbelia - : : ee
Pittosporum — - - : = Burtonia - - : : = i
Comesperma — - : : - 2 Daviesia - : : : - il
Eriostemon — - Z zs ] Gastrolobium : Z : 1
Plagianthus - - - - 1 Templetonia - - - -
Commerconia - - 2 38) Ptychosema — - x : 2 |
Hannafordia - - = i Swainsonia E : a
Seringea - - - - 38 Kennedya - : : -
Macgregoria : = = Cassia - : : Z - 10
Adriana - = = : e 1 Petalostylis — - : s E l
Ficus — - : 2 : - Acacia (phyllodinez) “ ay od
Casuarina = - - : 1 Loudonia = : : : 1
Atalaya - - - - el Haloragis - - 3 - 8
Heterodendron S 2 : l Calycothrix — - = : 1
Diplopeltis z : : : 1 Thryptomene - : = : 2
Dodonwa - - ae Beeckea - : : 2 :
Stackhousia — - : : a= oO Melaleuca z : : - 8
Ptilotus - : - : 2 1H Eucalyptus x - : - 10
Rhagodia = : : a? 62 Cryptandra — - - : - |
Dysphania — - - - - 2 Didiscus - - - - ~ 2
Enchyliena - - - < 1 Actinotus : - z : 1
Babbagia - - - 1 Exocarpos 3 2 2 = 1
Muehlenbeckia - - 2. fl Anthobolus — - 2 : =e
Gryostemon — - - - - Jd Santalum F . “ ee
Codonocarpus - - - - 1 Loranthus - = - > so
Pimelea - - - - 2. YQ Grevillea 5 : : ES)
Brachysema — - : : 1 Hakea = - 7 7 E . 4

128 HORN EXPEDITION—BOTANY.

Genera. Seale Genera. Sees,
Pomax - . - ae Be Velleya - : = : 7
Brachycome — - - : el Polymeria - - - - 2
Minuria - - - ay etD, Duboisia - - : = > ill
Calotis — - : : - 10 Prostanthera - = = =
Vittadinia - - 5 = 74 Spartothamnus - - - 2
Pterigeron —- . - ees) Neweastlia — - : : . 2
Txioleena - : - = el Dicrastylis = - - - 9§O
Podolepis - : : = ¥ Eremophila — - : : = if
Waitzia - = = - = Myoporum - - . sil
Helipterum — - - - - 10 Halgania - = - = ¥
Rutidosis - - - = il Styphelia - - - ee!
Millotia - - - - - 1 Elacholoma — - - - - l
Myriocephalus - ; : = 1 Callitris - A Z : 5 iT
Angianthus — - = =ibpvil Macrozamia — - - = » J
Gnephosis : - - 2. I Thysanotus — - - - - l
Eriochlamys © - - ee! Corynotheca — - - - - 1
Calocephalus - = = = Xerotes - - - : reso)
Erechtites = - - - 2 Xanthorrhea - - - > i
Tsotoma - - - - = pal Livistona - - - 2 lal
Candollea - - - =\, | al Centrolepis — - - - = ah
Bruonia - - = - ee fol Spinifex - - - - =" yall
Leschenaultia - : - =U a Neurachne - . ise ate wl
Catosperma — - - - =e 1 _ Triraphis - - - - 2
Serevola - - - - =: | Astrebla - - - - =a
Goodenia - - - = 15} |

The more modern facies of the Eremian flora is shown not only by the high
percentage of exotic species (twenty in the Larapintine flora ; whilst for the whole
Eremian flora in South Australia I have stated it to be, writing in 1888,* 16-8, thus
indicating an increase in the northern area, as might be expected as we approach
their centres of dispersal), but also by the wide dispersal of a large number of them,
which thus evince a quality of accommodating themselves to a great variety of

climatic and other physical influences,

The majority of the plants possessing burr-like, pungent, pointed or adhesive

fruits belong either to exotic species or to endemic species of exotic genera, and

* Austr, Assoc, Ady. Science, vol. i., p. 317.

HORN EXPEDITION—BOTANY. 129

are widely dispersed over the low-level tracts, though some ascend to high eleva-
tions on the rocky country. The rare instances of species with such aids for
dispersal, which are local and saxatile, are Achyranthes aspersa and Plumbago
Zeylanica. The only species of endemic genera whose fruits possess clinging appen-
dages, which would aid their transport by the agency of animals, belong to Cadotis,
all of which inhabit the lowland areas. The feathery achenes of some Composite,
except perhaps in Sevecto, are not sufficiently buoyant to be useful aids in their
distribution unless under the influence of very high winds, which were not at all
experienced during our stay. The same remark applies to the winged fruits of
Atalaya, ete., to the coma-bearing seeds of the Asclepiads, Hibiscus, ete., and to
the winged seeds of Casuarina, Tecoma, ete.

The number of species bearing edible fruits is absolutely few. They belong
for the most part to species of endemic genera, and, with the exception of Anfho-
bolus and Styphelia, which are saxatile and very rare, are widely diffused over the
low levels. In Afelothria and Cucumis we have two exotic forms widely diffused,
and in Zrema, another exotic, saxatile and rare. We know too little of the
natural foods of the native birds to make them accountable for the diffusion of
plant species, the seeds or fruits of which they may live on. The emu, which is
actually known to be an agent in the dispersal of Saxfalum, may also play the
same 7d/e in regard to other species yielding pulpy fruits. The parrots and pigeons
during the time of our sojourn were feeding on graminaceous seeds. The little
Dicaeum hirundinaceum \ives chiefly on the berries of Loranthus sfp., and in
consequence the distribution of the bird is coterminous with that of its food-plants.
Tasmania and Kangaroo Island, where the bird is absent, do not possess a single
species of Zoranthus. Thus, though among the lowland vegetation there are many
species possessing advantages for their dispersal, yet among the saxatile vegetation
such properties are almost wholly wanting. The details are set forth in the
following table :—

: tat
Genera Exotic. Genera

Exotic, Enddinic, Endemic. deh
(a) Burr-like Fruits—

Triumfetta micracantha — - - xX - Very rare.
Tribulus terrestris — - - xX - - Lowland, wide-spread.
Achyranthes aspera - - xX - - Saxatile, local.
Bassia, spp. - - - - x - Lowland, several wide spread.
Salsola kali - - - XxX - - Lowland, wide-spread.
Daucus brachiatus — - - xX - - Lowland, wide-spread.
Glossogyne tenuifolia - xX - - Lowland, common.

130

Bidens tripartita -
Calotis, spp. - : \

Cynoglossum Drummondi -

Andropogon Gryllus
Anthistiria ciliata — - -

Anthistiria avenacea =
Tragus racemosus — - -

Aristida, spp. - - -

Chloris acicularis = 2

Stipa scabra — - : z

(6) Adhesive Fruits—

Cleome viscosa :
Boerhaavia diffusa - =

Boerhaavia repanda :
Plumbago Zeylanica -

Siegesbeckia orientalis

(¢) Fleshy Fruits—

Rhagodia spinescens -
Rhagodia nutans — - -
Enchlyzena tomentosa -
Trema cannabina — - .
Anthobolus exocarpoides. -
Santalum, spp. - - -
Melothria maderaspatana
Cucumis chate - -
Loranthus, spp. -
Myoporum Dampieri
Sceevola spinescens -
Jasminum, spp. - -

Clerodendron floribundum

Sp.
Exotic.

X

x

Genera Exotic.
Sp.
Endemic.

x

Genera
Endemic,

x<

HORN EXPEDITION—BOTANY.

Distribution.

Lowland, rare.

Lowland, mostly wide-spread.

Saxatile, common.

Lowland, not rare.

Lowland, wide-spread,
saxatile.

Lowland, wide-spread.

also

Lowland, exceedingly diffused.

Lowland, wide-spread,
partly saxatile.
Lowland, common.

Lowland, rare.

and

Lowland and saxatile, wide-

spread.

Lowland and saxatile, wide-

spread.

Saxatile, local.

Lowland, wide-spread.

Lowland, common.
Lowland, common.
Lowland, common.
Saxatile, rare.

Saxatile, very rare.
Lowland, common.

Lowland, common.

Lowland, not uncommon.

Lowland, common.
Lowland, common.
Lowland, common.

Lowland.

Lowland, not uncommon.

HORN EXPEDITION— BOTANY. 131

Genera Exotic.

. Genera dick ;
Sp. Sp. Sea Distribution.
Exotic. Endemic. Endemic.

Spartothamnus teucriifolius - - x Lowland, not uncommon.
Spartothamnus puberulus - - xX Saxatile, very rare.
Carissa Browni : = SUMED eae Lowland and saxatile.
Solanum, spp. - - - - XxX - Lowland, wholly or in part.
Styphelia Mitchell - - - - X& Saxatile, very rare.

The colonising power possessed by the Eremian plants has had freer scope to
exercise itself in the unoccupied tract of the low levels on the reduction in size of
its lake-basins and water-ways than was possible in the more stable external
regions. Another feature pointing in the same direction is the high state of
specific luxuriance in many of its exotic genera ; and that a process of differentia-
tion sees to be in progress, because of the local racial characters exhibited in
some genera and species. Further, the many monotypic genera, which are for the
most part offsets from Australian types altered by new surroundings, show no

singularity which may be attributed to a high antiquity.

An indispensable property of the Eremian plants is that of rapid germination,
so as to take advantage of the rare opportunities when the physical and hygro-
metric conditions of the soil are favourable and quite irrespective of temperature.
Moreover, the long droughts intervening between the favourable periods necessitate
another quality in their seeds—that of resistance to long exposure. Individual
tenacity of life is another essential condition of maintaining a foothold in the dry
or desert zone.

The balance of 218 species in category III. are either actually Autochthonian
or Euronotian, or are related species, and as a whole may be viewed either as
residues of a common Australian flora, or as modified descendants therefrom.
Here belong all the saxatile species of endemic genera, as also others of endemic

genera inhabiting the low-level tracts.

The Larapintine area, in common with the rest of Australia, contains repre-
sentative genera of that primitive flora which marks the close of the Cretaceous
and the early stages of the Tertiary period, as has been made known chiefly by
the researches of Baron von Ettinghausen (Contributions Tertiary Flora of Aus-
tralia, Mem. Geol. Surv., N.S.W., 1888). The forms belonging to this type of
vegetation, which are present in the area, are /icus, Loranthus, Pitlosporum,
Santalum and Cassia, in association with Cadlitrts, Casuartna, Grevillea, Hakea,
Eucalyptus, and phyllodineous Acacie@, now restricted to Australia. Most of the

lia

132 HORN EXPEDITION—BOTANY.

first series, when viewed by their present geographic distribution, are considered
Oriental; but in regard to their distribution, in time they belong to a Cosmopolitan
flora, which originated in Late Cretaceous times in Europe, North America, and
Australia; hence their modern representatives, except the exotic species, may
actually be descendants of primitive Australian species, and not modified immi-

grant forms.

The isolation of many of the Larapintine species and the sporadic occurrences
of others are facts suggestive of the opinion that they are modified descendants of
a primitive flora. Thus the fan-palm, Zivistona Maria, is known by one colony
only, estimated to comprise not more than a hundred mature individuals, and
though seedlings are numerous, yet very few juvenescent examples were observed ;
also on the banks of the Finke River, below its junction with Palm Creek, con-
siderable numbers of young plants were seen, whilst the number of full-grown
trees does not exceed a dozen. It may therefore be inferred from these circum-
stances that a powerful agency is at work repressing the increase of individuals
and endangering the very existence of the species. The grass-tree, Yanthorrhaa
Thorntoni, is restricted to a belt of sandy country of about seventy miles long and,
thirty miles wide. Svrachysema Chambersii is gregarious, though usually the
colonies are extensive. Xerofes dura is known in two colonies of a very limited
nuinber of individuals, some fifty miles apart. Szvainsonia canescens occurs in two
colonies, occupying a few square yards, seventy-seven miles apart. Gas¢rolobium
grandiflorum is very local and the colonies widely separated. Goodenia Horniana
occurs in two colonies of few individuals, separated by 100 miles. eckea foly-
stemonea is restricted to two localities, 260 miles apart. Whilst Actinotus
Schwartsit, Didiscus Gillene, Prostanthera Schultsit, Styphelia Mitchelli and a few
others are restricted, so far as known, each to a circumscribed habitat. Moreover,
some of the endemic species of exotic genera, and even some immigrant species,
occur in small single colonies. Of the former may be mentioned Gvammiitts
Reynoldsi and Oftelia ovalifolia, and of the latter Heleocharis capitata, Lipocarpha
microcephala, Psilotum triquetrum, Adiantum hispidulum, and Aspidium unitum.
As the majority of these exemplar species are so conspicuous, or of others because of
the particularity of their habits, there cannot be room to doubt the general appli-
cability of the opinion which I have formed as to their sparse distribution, And
though a suspicion may be raised that they are stragglers from outlying regions,
yet our knowledge of their extra-limital distribution forbids such an explanation.
Thus for the majority of the species the Larapintine region is their metropolis,
whilst others which range beyond it are equally sporadic in their occurrences. In

the latter category the following selected species may serve as illustrations :—

HORN EXPEDITION—BOTANY. 1133

Sida tnclusa, N.A., Hammersley Range; S/da lepida, N.W.A., De Grey
tiver, Gascoyne River; Clayfonia spergularina, Nicholson River, Gulf of Car-
pentaria and Cape’s River, Queensland. Pé/ofus parvifolius extends to the
southern confines of the Central Kremian region and crosses into New South
Wales, but is rare in these external areas ; Lrachysema Chambersit is known also
from Barrow Range and in N.A.; AZrbelia oxyelada, Victoria River, Arnheim
Land, Hammersley Range ; Burtonta pfolvsyga, the only external locality is Mount
Morphett on the confines of Burt Plain; Szwacnsonta canescens is known at two
other localities, Swan River and Nickol Bay; Cassca glutinosa at Attack Creek ;
Grevillea ertostachya, Murchison River, Champion Bay, Nickol River; Cad¢osperma

Mueller’, Victoria River and River Thomson in Queensland.

From the known habits of the exotic species inhabiting the rocks and pools of
the Larapintine gorges and ravines, it may be inferred from the circumstance of
their local occurrence that they, as well as the Australian species previously
quoted, are on the verge of extinction within the Larapintine area. It is
satisfactorily established, on geological and biological data, that from Pliocene
times the rainfall in Central Australia has greatly diminished ; so that, if species
of plants were introduced to the region during the duration of the favourable
climatic conditions, it is not unreasonable to suppose that those less adapted to
increasing desiccation would disappear, or continue to live only in those restricted
areas where the struggle for existence would be the least severe. Hence, the
deep-shaded gorges and escarpments, particularly those with perennial water-flows
(the rock-structures in the George Gill and Krichauff Ranges are especially
favourable), have become harbours of refuge to the few survivors of an extinct

population.

The most ancient species among the living generation of Australian plant,
is Callitris robusta, Which inhabited Central Australia coeval with the large extinct
mmarsupalia, as they are associated in the Pliocene clays at Lake Callabonna.*
However, the species is absent in a living state from the Central Eremian regions
and does not appear in a northerly direction till the Larapintine table-land is
reached.

The minor influences checking reproduction of the species of the endemic
flora as consequences of increased aridity are :-

(1) The general absence of perennial streams and the salinity of the surface

stores of water, which increases with the prolongation of the rainless season.

* Tate, Trans. Roy. Soc. 8. Aust., vol. xviii., p. 195, 1894.

134 HORN EXPEDITION— BOTANY.

Thus Palm Creek, at the time of our visit, contained a slight flow of fresh water,
whilst the waterholes in the channel of the River Finke, in the Glen of Palms,
was undrinkable ; the latter circumstance may explain the rare occurrence of the
fan-palm in the Glen of Palms, though it is in near proximity to the main colony
at the former place.

(2) Frost. The main flowering period follows on that of the chief precipita-
tion of rain, which usually takes place in January or February ; so that, by the
time the arboreous and shrubby vegetation has regained its vigour and the
flowering condition reached, the season of nightly frosts has been entered upon.*
However, before this has come to pass the annual vegetation has for the most
part run its course. Though the effects of frost were not general, yet in the case
of the following species (Casséa venusta, Santalum acuminatum, Clerodendron
floribundum), growing in open places they were most marked, not only the flowering
buds killed, but the foliage presented a withered appearance. To the same cause
I attribute the not infrequent absence of mature seeds, either by checking the
perfection of the sexual organs or by killing-off those insects (and certainly at the
time of our visit insect life was feebly represented) which are the agents of
pollinisation.

Some of the Larapintine plants may be regarded as connecting links between
the Autochthonian and Euronotian floras, and in some species to indicate the
horizontal plane of divergence from the primitive stock. Among restricted species
Xanthorrhea Thorntont, though occupying an insular position, is the centre of a
semi-circumferential distribution of the genus, from the south-west by south to east
and north-east of the continent. The same remark is applicable to Commerconia,
spp., Axthobolus exocarpoides, Backea polystemonea, Actinotus Schwarsit and
Macrozamia Macdonneltt.

Flibbertia glaberrima stands alone as an extralimital species in the section
Hemihibbertia, otherwise Autochthonian. It ranges from Queensland through
the Larapintine area (its metropolis) to Mount Olga and Everard Range.
Gastrolobium grandiflorum is the only extra-Autochthonian species of this large
genus, and radiates from the Larapintine region to Attack Creek and Neweastle
Waters on the north, to the adjacent parts of Queensland and New South Wales,
and to the Eremian portion of West Australia. Lrachysema Chambersi@ is a link

between the home of the genus in West Australia and the northern stations of a

* The minimum thermometric readings were almost always below freezing point, and the greatest cold regis-
tered was 15 deg. F.

HORN EXPEDITION—BOTANY. 135

few species ; in a south-west direction this species extends to Barrow Range. The
same remarks apply equally well to AZirbe/ta oxyclada, Burtonia polysvga, Tsotropts,
spp., Leschenaultia divaricata and Styphelia Mitchelli. In this connection the

genus Jacksonia is conspicuously absent from the Larapintine basin.

Conclusions.—The distribution of the constituent elements of the Larapintine
flora and their exoteric relationships, taken in conjunction with the physiographic

changes that have taken place within the area, lead to the conclusions that :—

1. The Larapintine tableland was isolated, except perhaps in a northerly
direction, during the deposition of the marine sediments constituting the Rolling

Downs system (Upper Cretaceous).

2. The marine submergence was replaced by a lacustrine area during the

deposition of the Desert Sandstone (Supra Cretaceous).

3. A cosmopolitan flora prevailed at this period, which continued into Paleocene

times.

4. The area occupied by the lacustrine area of the Desert Sandstone period

was somewhat reduced, yet high pluvial conditions continued into Pliocene times.

5. In Post-Pliocene times a high state of desiccation was reached, which has
continued till to-day. The cosmopolitan flora became largely extinct, and its
place occupied by an Oriental immigration, more especially over the previously-

submerged areas.

4. Previous EXPLORATIONS.

The first botanical exploration of the Larapintine region was by J. MAcpouaLt
Sruart, who collected during his traverses from the Finke River to the McDonnell
Range in 1860-62. The plants were determined by Baron von Mueller, and their
enumeration published as an appendix to the “Journals of J. MeD. Stuart,”
London, 1864. Of the fifty-two species catalogued, thirty-two were gathered
within the area which forms the subject of this report ; seven of them were scien-
tifically unknown till described by F. von Mueller in vols. ii. and iii. of the
“ Fragmenta Phyt. Aust.”

Ten years later Ernest GILES geographically explored the Larapintine region
to the westward of the Finke River, and made extensive botanical collections. A
list of the species, furnished by Baron von Mueller, was published as an appendix

to Mr. E. Giles’ “Geographic Travels in Central Australia,” 1872-74 (Melbourne,

136 HORN EXPEDITION

BOTANY.

1875). It contains the names of 254 species, of which 114 belong to the Larapin-
tine flora, but as seventeen had already been recorded from Stuart’s material, the
actual gain in numbers is reduced to ninety-seven, making a total known at this
time to be 129.

Cotemporaneously with Giles, W. C. Gossr crossed the western confines of the
Larapintine region in his traverse from Central Mount Wedge and Mount Liebig
to Mount Olga, and though he collected plants during his explorations, yet the
only record as regards this particular region is that of “ grass trees ” (s7c) in the

neighbourhood of Glen Edith.

The Rev. H. Kemps, of the Mission Station at Hermannsburg, made succes-
sive collections of plants in his neighbourhood, which were determined by Baron
von Mueller, and their names were communicated in two lists to the Royal Society
of South Australia, and published in its Transactions, vol. iii, p. 129, 1880, and
vol. v., p. 19, 1882. The result of Mr. Kempe’s investigations, as far as numbers
are concerned, is, at the latter date, 287 species, and of these 219 are records of

additional species, making the total known for the region 348,

In 1889 Mr. 'TierKens traversed the northern part of the Larapintine region,
from Alice Springs to its western limit, and added fifty-eight species, including
five new to science, to the Larapintine flora. A list of the plants collected by
him is published in the Trans. Roy. Soc. 8. Aust., vol. xii, pp. 94-109, 170-171,
1890.

Lastly, from collections received by Baron von Mueller, during the period
intermediate between the two last-named, from the missionaries at Hermannsburg,
the officers attached to the Telegraph Stations at Charlotte Waters and Alice
Springs, and from other residents within the region, he has from time to time
published diagnoses of new species and records of others previously unknown in

this region.

From these various sources of information I have compiled the accompanying
List of Plants, adding my records of localities of those plants actually observed in
life. Since the return of the Expedition Mr. F. J. Gillen, of Alice Springs, has
forwarded a collection of flowering plants gathered in his immediate neighbour-
hood ; from it I am able to insert “ Alice Springs” as an additional locality for

several species.

The number of species known previous to the advent of the Horn Expedition

was 502, which is now increased to 614. The additions are comprised of ; new

HORN EXPEDITION—BOTANY. NS

species, 8; new for South Australia, 16: new for the region, 112. Threlke/dia
proceriflora, gathered at Adminga, in the Central Kremian region, is another

addition to the provincial flora.

To Baron von Mueller I am indebted for assistance in the determination
of a few critical species, as well as for certain notes which are incorporated in the
following enumeration of plants, and the authorship of which is in each case

indicated.

5. ENUMERATION OF THE PLANTS OF THE LARAPINTINE REGION.

[Index to signs :—* saxatile species, || exotic species, ! signifies that the species

was observed at the station indicated. |

DILLENIACEA.

* HIBBerRTIA GLABERRIMA, /. v. JZ. Restricted to rocky ravines; Glen of
Palms (E. Giles) and its tributary Palm Creek! in Krichauff Range ; Reedy and
Bagot’s Creeks! in George Gill Range; Redbank Gorge by Mount Sonder ! and
srinkley Bluff! (Stuart) in McDonnell Range. Extends south-west to Mount
Olga (Tietkens) and Everard Range (Elder Exped.).

CAPPARIDEA.

||CLteomeE viscosa, Ziané. Extends from Macumba River to McDonnell
Range, as at Glen Helen!; chiefly in the alluvial valleys and by creek margins,
but ascends the rocky declivities to high altitudes, as near the summit of Mount
Gillen !

*|Capparis spinosa, Zéunvé. A lax shrub, attaining to eight to twelve fect
high, growing in the shade of fig trees ; confined to rocky ground and ascending to
considerable altitudes above the river plains. Ipilla Gorge!; Ilara Water! ;
Palm Creek! in Krichauff Range (Kempe); Gill’s Pass!; Alice Springs!; near

Mount Sonder (Tietkens).

Capparis Mircnenui, Zinvd/ey. A small tree, widely dispersed, but never
gregarious, chiefly on loamy ground, becoming shrubby on rocky ground. Hen-
bury !; Ipilla!; Tempe Downs!; south side of George Gill Range !; source of
Carmichael Creek !; Upper Finke and tributaries near Mount Sonder!, ete. ;
McDonnell Range and Mount Udor (KE. Giles); Hermannsburg (Kempe) ; Dash-

wood Creek (Tietkens).
18

138 HORN EXPEDITION—BOTANY.

CRUCIFERA.

Erysimum LAsiocarpum, /. v. JZ, On loamy flats; Henbury!; junction of
Finke and Palmer Rivers; River Hugh at Alice Well!; Alice Springs !.

STENOPETALUM veELUTINUM, /. v. AZ. Laurie’s Creek!; slopes of Mount
Francis, Belt Range! ; Hermannsburg (Kempe).

STENOPETALUM LINEARE, 7. 57. Hermannsburg (Kempe).

STENOPETALUM NUTANS, / v. JZ. Alluvial flats and loamy plains. ITIpilla! ;
Glen Helen!; Horn Valley !* ; Burt Plain!; Bond Spring (Tietkens); Hermanns-
burg (Kempe).

CAPSELLA OCHRANTHA, /. v. JZ. Mount Sonder (Tietkens).

Lepipium rotunpum, De Cand. Loamy flats in Horn Valley!; near Her-

mannsburg (Kempe).

LePIDIUM PHLEBOPETALUM, / v. JZ. Alice Springs! (C. Giles); Glen Helen !
(Tietkens) ; Stuart’s Pass!; Ooraminna Pass and Waterhouse Range !; Hermanns-

burg (Kempe).

LepPipIuM PAPILLOSUM, / v. JZ Common throughout the region, chiefly on
loamy plains, as at Hermannsburg (Kempe); also on the escarpment of George
Gill Range !.

|| LepIDIUM RUDERALE, Zinné, Common in most places by creeks, Henbury,
&e.!; Hermannsburg (Kempe).

VIOLACEA.

*|| HYBANTHUS ENNEASPERMUS, / v. JZ. Slopes of Mount Tate!; Alice
Springs!; McDonnell Range (KE. Giles); near Hermannsburg (Kempe) ; Gill’s
Creek (Tietkens).

PIT TOSPOREA.

PIrrosPORUM PHILLYROIDES, Ye Cand. Sparsely dispersed throughout the
region. Sullivan Creek !, Illara Water!, south side of George Gill Range, Burt

Plain !, ete. ; Gosse’s Range (EK. Giles); Hermannsburg (Kempe).

* This station refers to that part of the valley between Goyder Pass and Finke Gorge.

HORN EXPEDITION—BOTANY. 139

DROSERACEA.

Drosgra Inpica, Zivné. Marshy ground at Reedy Creek !; Stuart’s Pass !;

Conlin’s Lagoon near Heavitree Gap !; Glen Farewell and Laura Vale (Tietkens) ;

5)

Finke River (Stuart) ; also, wet banks of the River Stevenson !.
| Drosera Burmanni, Vah?. McDonnell Range (KE. Giles); Glen Farewell
and Laura Vale (Tietkens).
ELATINEA.

(Evatine Americana, Arnott, Marshy ground in Stuart’s Pass, near

Brinkley Bluff!, and in gorge of Bagot’s Creek in George Gill Range !.

| BerGia AMMANNIODES, Roxburgh. Margin of Conlin’s Lagoon, near Emily

Gap; Darwent Creek !; Carmichael Creek !; also River Stevenson }.

BrerGIA PERENNIS, 72 v. JZ Hermannsburg (Kempe), near Mount Sonder
(Tietkens).

HYPERICINA.

| Hypericum Japontcum, Zhunderg. Margin of Gully Waterhole near Tempe
Downs!; Reedy Creek !; Stuart’s Pass!; Mount Sonder and west of McDonnell

Range (Tietkens).
POLYGALEA.
|| PotyGaLa Cuinensis, Ziznzé. Alice Springs (C. Giles).

ComMESPERMA syLvestrE, Lindley. Between McDonnell and Gill Range
(KE. Giles).

ComusperMa visctpuLuM, / uv. JZ McDonnell Range (1. Giles).

RUTACEA.

* EriostEMON ARGYREUS, /& v. AZ. and Zate. Near Mount Sonder (Tietkens).

ZYGOPHYLLEZ.

ZYGOPHYLLUM ApicuLATuM, /& v. JZ. Mlamurta Soakage, in James Range! ;

mallee scrub by banks of Upper Finke, under Mount Sonder! ; Hermannsburg

oD

(Kempe).

1SA

140 HORN EXPEDITION—BOTANY.

ZYGOPHYLLUM IopocARPUM, /, v. AZ, Stony ground, east end of George Gill
Range, and by Upper Finke near Mount Sonder! ; Alice Springs (C. Giles).

ZYGOPHYLLUM PRISMATOTHECUM, /. v. AZ. River Finke at Idracowra! ; lime-
stone slopes of Mount Sonder !.

ZYGOPHYLLUM AMMOPHILUM, / v. AZ. River Finke at Crown Point, Henbury
and Idracowra! ; sources of Rudall’s and Darwent Creeks! ; Finke Gorge and
Horn Valley! ; Ooraminna Pass! ; banks of the River Hugh at Alice Creek! ;
Alice Springs (C. Giles) ; Hermannsburg (Kempe).

ZYGOPHYLLUM FRUTICULOSUM, De Cand. Mount Harris (Tietkens); Her-
mannsburg (Kempe).

ZycorHyttum Howirru, / v. AZ. River Finke at Engoordina and Crown
Point! ; also Lilla Creek at Mount Humphries !, the most northern stations of the

species.

|| TRIBULUS TERRESTRIS, Z7v7é. Common on loamy and sandy soils through-
out the region !. Recorded by Kempe.

TripuLus macrocarpus, / v. JZ. Plain at foot of Belt Range! ; also sand-
hills from Mount Squire to the Goyder River !, near Charlotte Waters (Kempe).

TripuLus Astrocarpus, /& v. JZ. No locality (Tietkens).

GERANIACEEZ.

Eropium cyGnorum, /Vees. Rich loamy plains; south side of George Gill
Range!; Vale of Tempe! ; Horn Valley !, and Conlin’s Lagoon! ; Hermannsburg
(Kempe).

| Oxanis cornicuLaTa, Zinné. Damp shady rocks and creek banks; Reedy
Creek Gorge! ; gorge of the Darwent! ; deep ravine of Mount Tate !, by Mount
Sonder ! (Tietkens) ; Stuart’s Pass !, Alice Springs (I. J. Gillen !).

Macerecoria RACEMoSA, / v. AZ. McDonnell Range (KE. Giles); Lake
Macdonald (Tietkens). Extends to Ryan’s Well, ninety miles north of Alice
Springs (F. J. Gillen !)

MALVACEA.

= ' eae : ee a eae
LAVATERA PLEBEIA, Sims. Banks of the River Finke in Finke Gorge! ;

Hermannsburg (Kempe).

HORN EXPEDI'LION— BOTANY. 141

| Manvastrum spicatum, 4. Gray. Widely spread from Oodnadatta to

Burt Plain !, Hermannsburg (I<empe).

PLAGIANTHUS GLOMERATUS, Lextham, Lake Macdonald (Tietkens) ; near
Hermannsburg (Kempe).

Sipa corrueata, Lindley. Widely spread. Sullivan’s Creek !, about Tempe

Downs !, valley of Carmichael Creek !, slopes of Mount Tate! Gosse and

McDonnell Ranges (KE. Giles) ; Hermannsburg (IXempe).

Stipa vircata, Afooker. Sand-plain between Glen Edith and Carmichael

Creek !, slopes of Mount Tate !, Hermannsburg (Kempe).

* SIDA CRYPHIOPETALA, /. v. AZ. A lax erect shrub up to six feet high,
growing on rock-slopes and ravines at Glen Helen and Finke Gorge, Palm Creek,
Palmer River, Reedy Creek, Darwent River, Stuart’s Pass!; Brinkley Bluff
(Stuart) and McDonnell Range (KE. Giles) ; Alice Springs (I. J. Gillen !).

*Sipa prerropuita, 7 v. M. McDonnell Range (K. Giles).
|Sipa ruomuiroura, Zivné. Wermannsburg (Kempe).

Stipa incLusa, Bentham. Sandy loam flats, Upilla, Bagot’s Creek, Carmichael
Creek, and Ooraminna Pass! ; McDonnell Range (EK. Giles); Warman Rocks and

Engoordina (Tietkens).
Sia vepipa, / v. JZ, Hermannsburg (Kempe).

SipA poporpeTaLta, /. v. AZ, and Tute. LU pilla Gorge in James Range! ;
Penny’s Creek in George Gill Range!; Glen Helen and Warman Rocks
(Tietkens) ; Alice Springs (I. J. Gillen !).

* ABUTILON TUBULOSUM, S/ovker. Ranges near Hermannsburg (Kempe) ;
Sullivan’s Creek, Tempe Downs, Redbank Creck, Stuart’s Pass, and Mount
Gillen! ; Glen Helen and Laura Vale (Tietkens). Wide spread, Hermannsburg

(IXempe).

ABUTILON CRYPTOPETALUM, /. v. AZ, Wide spread, Hermannsburg (Kempe).
Stuart’s Pass !.

ABUTILON oxycArpuM, & v. AZ. ; vAR. with the sepals as long as the fruitlets.
Bed of the Finke between Henbury and Parkes Gap!; Ilpilla Gorge! ; Bagot’s
Creek ! and Stuart’s Pass !.

AputiILon Frasent, Hooker. Idracowra, east end of George Gill Range and

Horn Valley !. Widely spread, Hlermannsburg (ICempe).

142 HORN EXPEDITION—BOTANY.

ABUTILON HALOPHILUM, / v. JZ. Glen Helen and Laura Vale (Tietkens).
ABUTILON MACRUM, /& v. JZ. Glen Helen!:.

Hisiscus MicrocHLHnus, / v. JZ. Bond Springs, near Mount Sonder !, and
Laura Vale (Tietkens) ; Hermannsburg (Kempe).

Hipiscus Pinonianus, Gaud. Lake Macdonald (Tietkens). Var. with
leaves shortly lobed; Ipilla Gorge, slopes of Mount Tate, Darwent River Gorge
and Mount Gillen !.

Hisiscus Farracet, / v. JZ McDonnell Range (E. Giles); Upper Finke
and tributaries by Mount Sonder! ; near Hermannsburg (Kempe) ; banks of the
Palmer River at Illara Water !.

* Hisiscus Sturtu, Hooker. Stuart’s Pass! ; slopes of Mount Tate! ; rocks

near Hermannsburg (Kempe). Var. with broadly oval leaves, Belt Range !.

Gossypium Srurtu, / v. JZ. Gosse’s and McDonnell Ranges (KE. Giles) ;
Mount Sonder !

Mereenie Bluff and Tempe Downs !.

; Ooraminna Pass! (Tietkens); Hermannsburg (Kempe) ;

GOssYPIUM AUSTRALE, / v. JZ. Glen Helen and Laura Vale (Tietkens) ;
Belt Range, Horn Valley, and east end of George Gill Range!; near Hermanns-
burg (Kempe).

STERCULIACEAE.

BracHycuHITon Grecori, / v. JZ. McDonnell Range, Mount Udor, and
Carmichael Creek (I. Giles). Sandhills between source of Laurie’s Creek and
Glen Edith, between Glen Edith and Carmichael Creek, Missionary Plain, south-

west of Gosse Range, and between Ooraminna and James Range |!.

| MeLHaANniA INcANA, Ffeyne. Kast end of George Gill Range!; Hermanns-
burg (Iempe).

| WatrHertIA Inpica, Zinné. Redbank Creek by Mount Sonder! ; banks

and channel of River Hugh in Stuart’s Pass! ; Glen of Palms (Kempe).

CoMMERCONIA KermPEANA, / v. JAZ Sandhills between Glen Edith and
Carmichael Creek! ; Watson Hills (Tietkens) ; near Hermannsburg (Kempe).
Extends to the Victoria Desert (Elder Exped.).

COMMERCONIA LOXOPHYLLA, / v. MZ. McDonnell Range (E. Giles).

HORN EXPEDITION—BOTANY. 143

* COMMERCONIA MAGNIFLORA, 7/2 v. JZ. Mount Sonder (Tietkens). Ranges
near Hermannsburg (Kempe); Glen of Palms (KE. Giles). Rocky ravines of the
River Palmer and of the George Gill Range !. Extends to Mount Olga (IE. Giles)

and Everard Range (Elder Exped.).

HANNAFORDIA Bissttui, #7. JZ Sand plain by the River Finke at Run-
ning Water! ; between Glen Edith (Tietkens) and Carmichael Creek! ; ranges

near Hermannsburg (Kempe).
SERINGEA COROLLATA, Sfee/z. McDonnell Range (E. Giles).
SERINGEA NEPHROSPERMA, /. v. AZ. McDonnell Range (KE. Giles).

SERINGEA INTEGRIFOLIA, 7. v. AZ Sand plain at Engoordina and at Running
Water! ; McDonnell Range (E. Giles).

TILIACEA.
Corcnorus Enpert, # v. AZ, North of McDonnell Range (Dittrich),

Corcuorus sipoipes, / v. JZ. McDonnell Range (Stuart) ; Hermannsburg

(Kempe).

TRIUMFETTA MICGRACANTHA, /) v. AZ. South-westward of the Finke River
(Schwarz) ; (F. v. M. in litteris, 10-9-1891).

EUPHORBIACEA.

EvupnorsiA MircneLiiana, orsster. Sandy margin of River Walker at

Tempe Downs !.

EvupPHorBIA ERYTHRANTHA, /2 v. JZ By Mereenie Bluff, east end of George
Gills Range, Belt Range !. Lake Macdonald (Tietkens).

Evupnorsia DrumMonpu, Zodssrer. Hermannsburg (Kempe); Mount Tate ! ;
Tempe Downs !. Mount Ziel (Tietkens).

EupHorBIA EREMOPHILA, Cuzningham. Belt Range and Mount Sonder!;
McDonnell Range (E. Giles) ; Emily Gap (Tietkens) ; Hermannsburg (Kempe).

PHYLLANTHUS THESIOIDES, Pevtham. Burt Plain (Tietkens) ; near Finke
River and Charlotte Waters (Kempe),

PHYLLANTHUS RHYTIDOsPERMUs, 4. v. JZ. Conlin’s Lagoon by Emily Gap |,
also. River Finke at Crown Point!; Hermannsburg (Kempe); Glen Flelen,
as P. minutiflorus (Yietkens).

144 HORN EXPEDITION—BOTANY.

PHYLLANTHUS FurRNRoHRI, /. v. AZ. Sandhills by the Finke River at
Engoordina and Idracowra !, by Bagot’s Creek, and by the Hugh at Alice Well !.
‘ar.—Hoary, leaves larger and somewhat distichous ; limestone surface in

Ooraminna Pass !.

PHYLLANTHUS LACUNARIUS, /. v. AZ. McDonnell Range (Tietkens) ; loam
banks of Darwent River !.

PHYLLANTHUS TRACHYSPERMUS, /. v. JZ. Mount Sonder (Tietkens).

ADRIANA TOMENTOSA, Gavd. McDonnell Range (K. Giles) ; Hermannsburg
(Kempe) ; Tempe Downs and north to Mount Sonder !; also Crown Point.

URTICACEA.

*|| TREMA CANNABINA, Loureiro. Redbank Gorge!, near Mount Sonder
(Tietkens) ; Stuart’s Pass !; Alice Springs (IF. J. Gillen !).

* Ficus PLATYPODA, Cunningham. On ail extensive rocky outcrops through-
out the Larapintine region! Recorded by Stuart, E. Giles, Kempe and

Tietkens.
* FICcUS ORBICULARIS, Cunningham. Glen of Palms (EK. Giles).

*|| PARIETARIA DEBILIS, G. /uster. Shaded rocks, Finke Gorge!; Palm
Creek !; ranges near Hermannsburg (Kempe).

CASUARINEA.

CasuARINA DecAIsNEANA, /. v. JZ, On sandhills throughout the Larapintine
region, reaching its southern limit a few miles north of Engoordina!; between
Ayers Rock and Mount Olga (Spencer), and between the Lilla Creek and

Erldunda (‘Tietkens). Recorded by Stuart, E. Giles, Kempe and Tietkens.

SAPINDACEA.,

ATALAYA HEMIGLAUCA, / v. JZ. McDonnell Range (E. Giles); Hermanns-
burg (Kempe); loam flats, Burt Plain!, Upper Finke by Mount Sonder !, south
side of George Gill Range !, Henbury !, and Chandler’s Range. Also at base of
Johnston’s Range, Engoordina and Mount Squire, Crown Point to the Goyder,

thence to Charlotte Waters ; Adminga to Blood’s Creek, and along the river-flats

HORN EXPEDITION—RBOTANY. 145

of the River Stevenson to Oolabarinna!; east slope of the Stanley Tableland in
Red Mulga Creek !.

HIkTERODENDRON OLEHFOLIUM, Desfontarnes. Burt Plain, Tempe Downs,

and Ilpilla Gorge !; Hermannsburg (Itempe).

* DipLopentis Sruarru, “2 v. AZ MeDonnell Range (KE. Giles); Mount
Sonder (Tietkens) ; stony slopes of Mount Tate !. Also Mount Conner (Tietkens).

* Dopon®a LANCEOLATA, /. v. JZ. On Mount Sonder!; Dashwood Creek

(Tietkens) ; near Hermannsburg (Kempe).

* Doponma prriotaris, / v. AZ, Alice Springs (E. Flint); Krichauff Range
(Kempe). Mount Gillen, Upper Finke by Mount Sonder, Glen Helen, Tempe

Downs, Ilpilla Gorge, and Chandler’s Range }.

| Doponma viscosa, Zinzné. Sandhills by the Finke at Engoordina, Idra-

cowra, etc. ! ; Hermannsburg (Kempe) ; Mount Sonder (Tietkens).

Doponma MAcROzYGA, /.v. JZ. Ilara Water (foliage only) !.

STACKHOUSIEA.

Sracknousta MuricaTa, Lindley. Gosse’s Range (Schwartz); near Her-

manusburg (Kempe).
* STACKHOUSIA VIMINEA, Smith. Stony slopes of Mounts Tate and Sonder !.

STACKHOUSIA MEGALOPTERA, 7. v7. JZ. McDonnell Range (I. Giles).

FRANKENIACEA.

| FRANKENIA Levis, Z7xnvé. Dry stony ground, Finke River (Stuart, Kempe) ;
limestone surface of south slope of Mount Sonder and between Ooraminna Range

and source of Francis Creek !. Conimon south from Engoordina !.

PLUMBAGINEA.

*\|PLrumpaco ZeiLanica, Linné. Hermannsburg (Kempe). Shady places

about rocks, Alice Springs and Simpson’s Gap |. ae

146 HORN EXPEDITION—BOTANY.

PORT ULACEA.

| Portunaca oLeracra, Zinné. Mount Zeil (Tietkens) ; by Mount Sonder !.

Common on sandhills by the River Stevenson.

PorTULACA FILIFOLIA, 7 v. AZ. Near Alice Springs and Charlotte Waters
(C. Giles) ; Ooraminna Waterhole (Tietkens). Sandbanks by waterhole on Arum-

bera Creek and in Stuart’s Pass !.

CLAYTONIA PrycHosPERMA, / v. JZ. Upper Finke River by Mount Sonder,
Carmichael Creek at Undoomoola Waterhole, and at Idracowra!; also between

Mount Daniel and Charlotte Waters, and south to the River Stevenson.

Crayronia Baronnensis, / v. AZ. McDonnell Range (E. Giles); Her-

mannsburg (Kempe). Not uncommon on sandy ground throughout the region !.
CLAYTONIA PUMILA, & v. MZ. Near McDonnell Range (E. Giles).
CLAYTONIA CORRIGIOLOIDES, /. v. AZ. Hermannsburg (Kempe).

CLAYTONIA SPERGULARINA, /. v. M/. Sandy bed of Upper Finke and its
tributaries by Mount Sonder, at Finke Gorge, and Glen of Palms! ; sandy margin

of Conlin’s Lagoon ; near Emily Gap !.

CARYOPHYLLEA.

| SPERGULARIA RUBRA, Pers. Sandy margin of Conlin’s Lagoon ; near Emily
Gap !.

POLYCARPHA SYNANDRA, /. v. MZ. Dashwood Creek (Tietkens); Alice
Springs (F. J. Gillen!). Common about the River Stevenson !.

|| Potycarpma Inpica, Zamarck. Glen of Palms (EK. Giles) ; Stuart’s Pass !,
Finke Gorge !, and Tempe Downs!. Also at the Goyder River!.

AMARANTACEA.
GOMPHRENA LANATA, 2. Lr, Hermannsburg (Kempe).

| ALTERNANTHERA TRIANDRA, Lamarck. McDonnell Range (KE. Giles) ; Her-

mannsburg (Kempe). Upper Finke by Mount Sonder !

HORN EXPEDITION—BOTANY. 147

ALTERNANTHERA NANA, &. Lr. Darwent River Gorge, Glen Helen, and
Upper Finke by Mount Sonder!; Hermannsburg (Kempe); Alice Springs (I. J.
Gillen !).

™ ACHYRANTHES ASPERA, Zinnzé. Stokes Pass, Goyder Pass and Painta
Spring!; Hermannsburg (Kempe).

Prinorus Larirouius, Rk. 4r. “Sandstone rocks” (Tietkens) ; sandhills,
Engoordina, Idracowra, Alice Creek and about the Lower Hugh River!; also

towards sources of Goyder River !.

Prinorus oBovatus, /. v. JZ. McDonnell Range (KE. Giles) ; Hermannsburg

(Kempe) ; occasionally on sandy ground throughout the region !.

Prinorus incANus, Potrve¢t. Hermannsburg (Kempe). Usually on stony
surtaces, Glen Helen! and Mount Sonder (Tietkens) ; Mount Gillen, Mount Tate,

and Tempe Downs!; also at the Goyder River !.

Prinorus ALoprcurorpEs, /. v. AZ. Widely spread on sandy soil; south side
George Gill Range, ete. !; Hermannsburg (Kempe).

1]

Pritorus Nopitis, / v. JZ. Not infrequent in bushy places, Ipilla Gorge },
Mount Sonder ! (Tietkens), ete. On rich soil in Krichauff Range (Kempe).

Prinorus wemisrerrus, / v. JZ. On stony ground, Ipilla Gorge and Mount
Francis ; also at the Goyder River and Giddea Creek near Oodnadatta !.

*Pritorus PARVIFOLIUs, /. v. JZ. Stony ground, Mereenie Bluff and Darwent
River Gorge!, Glen Helen and Mount Sonder!, Ooraminna Pass! ; also Mount
Squire and Crown Point, towards the sources of the Goyder River, Adminga
Creek, and by the River Stevenson !.

* Prrtorus EXALTATUS, Vees. West of Mount Sonder (Tietkens) ; common on
stony taluses, from Crown Point on the south to Belt Range on the north |.

Pritorus uELipreroipes, / v. AZ Alice Springs (F. J. Gillen !); sandy
plains about Hermannsburg (Kempe); Ipilla, east end of George Gill Range, and
Mount Francis |.

Pritorus Scuwarrzu, 2 v. JZ Near McDonnell Range (Schwartz); stony

) 1 ? | F RP » 1 > » » !

ground, Penny’s Creek !, Laurie's Creek !, Mount Tate!, Glen Helen!, Mount
Sonder !, as P. Zeucocomus (Tietkens), Stuart’s Pass |, gravelly knolls on Missionary
Plain about Harris Creek !.

*Pritorus Hoopu, # v. Jf Ipilla Gorge, Laurie’s Creek, Horn Valley

and on Mount Gillen !, Previously known only from Mount Olga (. Giles).
LDA

148 HORN EXPEDITION—BOTANY.

Evuxotus Mrrenenu, / v. JZ. Common along creek-margins, but ascending
hilly tracts as near summit of Mount Gillen!; stony tracts near Hermannsburg
(Kempe) ; Ooraminna (Tietkens); also frequent by river-channels from Crown
Point to Oodnadatta !.

SALSOLACEZ.

ATRIPLEX VELUTINELLUM, /. v. 47. Hermannsburg (Kempe).
ATRIPLEX NUMMULARIUM, Lindley. Hermannsburg (Kempe).
ATRIPLEX VESICARIUM, /Zeward. Hermannsburg (Kempe); Henbury !.

ATRIPLEX sponciosuM, / v. JAZ Hermannsburg (Kempe); common at

Crown Point and the Goyder and southward !.
RHAGODIA SPINESCENS, A. Brown. Hermannsburg (Kempe).

Ruacopia Nutans, &. Brown. Alice Springs (Flint); Hermannsburg
(Kempe) ; Sullivan’s Creek !.

CHENOPODIUM NITRARIACEUM, /& v. AZ. Upper Finke by Mount Sonder! ;
claypans at entrance to King’s Creek !.

CuENopopIUM AuRIcoMUM, Lindley. Hermannsburg (Kempe); south side of
George Gill Range !.

CueENopopium carinatuM, &. Zr. Alice Springs (C. Giles); Hermannsburg
(Kempe), Ilpilla Gorge !.

CHENOPODIUM RHADINOSTACHYUM, / v. J/. Laura Vale (Tietkens), Her-
mannsburg (Kempe), Ilpilla Gorge, Glen Helen, Stuart’s Pass, and on Mount
Gillen !. As C. stémudans at Mount Sonder (Tietkens).

DyYSPHANIA PLANTAGINELLA, / v. AZ. Alice Springs (C. Giles), Hermanns-
burg (Kempe); Finke Channel at Henbury, also at Crown Point, Glen Helen,
and on Mount Gillen !.

DysPHANIA LITORALIS, 2. Lrown. Upper Finke and tributaries by Mount

Sonder, and at Conlin’s Lagoon !; also by River Stevenson !.

Kocuia LANnosa, Zind/ey. Hermannsburg (Kempe), Alice Springs (C. Giles);
Laurie’s and Reedy Creeks !.

KocuHIA TRIPTERA, Bentham. Alice Springs (C. Giles) ; Stuart’s Pass !.

HORN EXPEDITION—BOTANY. 149

KociiaA BREVIFOLIA, R. Lr. Hermannsburg (Kempe).
IKKocHIA SPONGIOCARPA, 2. v. AZ. Laurie’s Creek !.
Kocnta rntantua, /. v. JZ. Hermannsburg (Kempe).

KocnrA vitLosa, Lindley. Hermaunsburg (Kempe); Tpilla and Stuart's

Pass !.

KKocuta sepirotia, “ v. JZ. South side of George Gill Range and plain

west of Carmichael’s Crag }.

IKocntaA APpHYLLA, A. Ly. Hermannsburg (Kempe), and loamy plains by

George Gill Range and Vale of Tempe !.

BaBBacta piprerocarrPa, /. v. JZ. Hermannsburg (Kempe); also at Goyder

River and Dalhousie Springs !

Bassa SCLEROLENOIDES, /2 v. J7. UWermannsburg (Kempe); also Crown
Point !.

BassiA UNIFLORA, / v. AZ. Lpilla Gorge !.

Bassia piacantua, 4. v. AZ. Hermannsburg (Kempe); also at the Goyder

River !

Bassta LANicuspis, #2 7. Jf. Hermannsburg (Kempe); also Charlotte
Waters (F. Giles).

Bassta Lurnmanni, /: 7. JZ Hermannsburg (Schwartz).

Bassta PARADOoxA, #2 v. JZ Hermannsburg (Kempe). Widely dispersed
throughout the region ; but more frequent about Crown Point, Goyder River and

southward !.
Bassta Quinquecuspls, /. v. JZ Ipilla Creek !; also at the Goyder River !.
BassiA Biren, v. J/. Base of Belt Range, Ipilla !.
Bassta ncuinopsita, 4. v. JZ. Upilla ; also at the Goyder River !.

ENCHYLENA TOMENTOSA, A. Lr. River Finke at Hermannsburg (Kempe)

and Running Water !; Alice Springs (I. J. Gillen !).

SALICORNIA RoBUsTA, 7. v. AZ Stony ground between James Range and
Alice Creek !.

SALICORNIA LEIOSTACHYA, Lentham. Hermannusburg (Kempe) ; Idracowra !.

150 HORN EXPEDITION— BOTANY.

| Sausota Kaui, Zixzxé. Common from Oodnadatta to Crown Point, thence

less frequent, but widely spread on loam flats and stony ground }.

FICOIDEA.

AIZOON ZYGOPHYLLOIDES, /. v. M. Var. with large rhomboid-ovate leaves,

larger flowers on longer pedicels, Chandler’s Range !; also at Crown Point !.

| ZALEYA DECANDRA, Burmann. Finke River (Kempe) ; Hope Valley beyond
Carmichael Crag, Ooraminna Waterhole; also Opossum Waterhole on the

Stevenson !.

|| TRIANTHEMA CRYSTALLINA, Vaf/. Stuart’s Pass! ; also Crown Point, valley
of the Goyder and southward |}.

TRIANTHEMA PILosA, /. v. AZ. Mount Sonder (Tietkens); River Finke
(Kempe) ; River Hugh at Alice Well ; also the Goyder and Stevenson Rivers !

| MotituGco uirta, Zhunderg. Mount Sonder (Tietkens) ; Stuart’s Pass, Horn
Valley, and Alice Well; also sandhills by the Goyder and Stevenson Rivers !

Mo.iuco oryGioipEs, /. v. AZ, Conlin’s Lagoon !

| MottuGgo cERVIANA, Séringe. UHermannsburg (Kempe); Glen Helen
(Tietkens). Sandhills and sandy creek beds, Idracowra, Henbury, by Mount
Sonder, Stuart’s Pass, and Alice Well!; Alice Springs (F. J. Gillen !).

POLYGONACEEZ.

| Potyconum pLeBetuM, &. Br. Mount Razorback (Tietkens) ; Hermanns-
burg (Kempe). Upper Finke by Mount Sonder, Finke Gorge, Conlin’s Lagoon,
and River Hugh at Alice Well !.

|| Potyconum minus, A/udson. With narrow lanceolate leaves, marsh at
Reedy Creek !.

MurxvenBecKIA Cunnincuamul, / v. 4 Hermannsburg (Kempe). South

side of George Gill Range and Conlin’s Lagoon !.

PHYTOLACCEA.
GyROSTEMON RAMULOSUS, Desfontaines. Glen of Palms (KE. Giles) ; Glen Edith
(Tietkens). Sandhills at Idracowra, and between the Hugh River and Engoordina ;

also south to the Goyder River}.

HORN EXPEDITION—BOTANY. 151

Coponocarpts coriniroLius, 7. v. J7. Glen Helen, Mount Sonder and Dash-
wood Creek (Tietkens) ; Hermannsburg (Kempe). By the Finke at Henbury, by
the Walker at Tempe Downs, and valley of Alice Creek, near Hugh River ; also

at the Goyder River !.

NYCTAGINEA.

| Borrnmaavia pirrusa, Zivzé. Glen of Palms (Kempe); Bond and Painta
Springs (Tietkens). Wide spread, on loamy flats and ascending to high elevations,

as on Mount Gillen !.

BoERHAAVIA PLANTAGINEA, Cavanilles, Lake Macdonald (Tietkens).

THYMELEZ.

PimeLeaA tTRIcHosTACHYA, ZLevdley. Gosse’s Range (I. Giles); stony rises,
Hermannsburg (Kempe); Ilpilla Gorge, east end of George Gill Range, and

Stuart’s Pass !.

PIMELEA MICROCEPHALA, 2X. Brown. Hermannsburg (Kempe); Horn Valley ! ;

also Crown Point to the River Stevenson !.

LEGUMINOSA.

BracnysemMa CramBersit, 7/2 v. J7. Between the Rivers Stevenson and Finke
(Stuart) ; McDonnell Range (E. Giles); sandhills, Rudall’s Creek (Kempe) ; at
Ipilla, between Laurie’s Creek and Glen Edith, and in the valley of Carmichael
Creek !; between George Gill Range and Lake Amadeus (Spencer !). Extends to

sarrow Range (Elder Exped.)

GASTROLOBIUM GRANDIFLORUM, /. v. JZ Glen of Palms (KE. Giles); Alice
Springs (//erd. F: v. AZ); south side of George Gill Range, and on Mount Sonder! ;
also at Ayers Rock (Spencer !).

Tsorropis ArropuRPUREA, 7/2 v. JZ Glen of Palms (E. Giles); and every-
where about Hermannsburg (Kempe); Alice Springs (F. J. Gillen !).

Tsorropis Wierevert, “7. AZ. Sandhills at Hermannsburg (Kempe).

*Mirpetia oxyctapa, / v. AZ. McDonnell Range (E. Giles); Krichautt
Range (Kempe); Bagot’s Creek and other ravines in George Gill Range ; rocky

slopes of Mount Tate !.

Lo2 HORN EXPEDITION—BOTANY.

*BurRTONIA PoLYZYGA, Bentham. McDonnell Range (E. Giles), south-west
slope of Mount Tate !.

Davigsia arTHROPODA, /. v. AZ. Sandhills, Eagle Plain near Palmer River !.

TEMPLETONIA EGENA, Sentham. Hermannsburg (Kempe); sandhills at

Idracowra, George Gill Range, and from Engoordina to the Hugh River !.

CROTALARIA NOVEHOLLANDI®, De Cand. var. Jasiophylla. Sandy soil
Ooraminna Pass !, near McDonnell Range (Flint, F. v. M. in litteris, 19-991).

CROTALARIA CUNNINGHAMII, #. 4r. Hermannsburg (Kempe); sandhills at
Idracowra, Carmichael Creek, between Ooraminna and James Ranges, and by the
River Hugh at Alice Well!; also Mount Humphries (Stuart) and River

Stevenson !

*|| CROTOLARIA MEDICAGINEA, Lamarck. Hermannsburg (Kempe); Bond
Springs, Mount Sonder and Laura Vale (Tietkens); sources of the Carmichael
and Darwent Creeks by Mereenie Bluff!; Horn Valley, Ipilla Gorge and Mount
Francis !; Paddy’s Hole in Hart Range (Watt !).

|| CROTALARIA INCANA, Zinné. Redbank Creek!, under Mount Sonder
(Tietkens).

CROTALARIA DISSITIFLORA, Bentham, var. eremea. Sandy ground and alluvial
flats, common!; McDonnell Range (Stuart); Laura Vale and Gill’s Creek
(Tietkens) ; Hermannsburg (Kempe); Upper Finke and tributaries by Mount

Sonder!; Alice Springs !.

Lotus ausrrais, Andrews. Hermannsburg (Kempe); Mount Sonder and
Laura Vale (Tietkens) ; Carmichael Creek and by Mereenie Bluff !.

PsoRALEA ERIANTHA, Bentham. UHermannsburg (Kempe); sandhills by the

Finke at Engoordina and between James Range and Hugh River !.
PsorALEA BALSAMICA, / v. JAZ. McDonnell Range (Stuart).

PsoRALEA PATENS, Lindley. Loamy flats subject to inundation and by river

banks, Upper Finke and tributaries, etc. !; Hermannsburg (Kempe).

|| INDIGOFERA LintFoLia, Refsivs. Hermannsburg (Kempe); Laura Vale
(Tietkens) ; bed of Ilpilla Creek, Mereenie Bluff, by Belt Range, Goyder Pass !.

| INDIGOFERA ENNEAPHYLLA, Zinzé. Hermannsburg (Kempe); near the

junction of the Rivers Finke and Palmer, and by Belt Range !.

HORN EXPEDITION—-BOTANY. 1553

| Inptcorpmra viscosa, Lamarck. Brinkley Bluff (Stuart); Hermannsbure
(Kempe); Bond Springs, Mount Sonder, &e. (Tietkens); Rudall’s Creek by

Mereenie Bluff, by Belt Range, Ooraminna Pass, also sandhills by River Stevenson !.
| Inpigorera uirsuva, Zzzvé. Mount Sonder (Tietkens),

INDIGOFERA MONOPHYLLA, De Cand. McDonnell Range (E. Giles); Laura
Vale and Gill’s Creek (Tietkens) ; Mereenie Bluff !.

INDIGOFERA BREVIDENS, Lentham. McDonnell Range (Stuart); Glen of
Palms! (i. Giles) and Krichauff Range (Kempe); Henbury, Ipilla, east end of
George Gill Range, slopes of Mount Francis and Mount Sonder, Finke Gorge and
Horn Valley, Stuart’s Pass and Mount Gillen !

I. coronillifolia, Cunningham, from McDonnell Range (Stuart), referred to
in Fl. Aust., vol. i, p. 201, belongs probably to the canescent variety of

TL. brevidens, which is restricted to rocky ground.
b fun)

PrycnoseMA TRIFOLIOLATUM, 7. v7. JZ Hermannsburg (Kempe) ; Ooraminna

Pass by Hell Gates, and between there and James Range !.

TrepHirosia spHmrospora, 7/2 v. AZ. Hermannsburg (Kempe); slopes of

Mount Tate and Ooraminna Pass !.

TEPHROSIA PURPUREA, Persoon. Stony ground, Hermannsburg (Kempe) ;

Tpilla, Tempe Downs, Reedy Creek, Stokes Pass Gorge, Horn Valley, Glen Helen
| ? I ? v d a) Ait) ’

Finke Gorge, and Stuart’s Puss !.

SWAINSONIA pPHACOIDES, Bentham. McDonnell Range (E. Giles) ; Hermanns-
burg (Kempe). Alluvial flats at Alice Well!

Swainsonta Burkert, / v. AZ McDonnell Range (EK. Giles); sandy and
loamy flats, Glen Helen !

SwAINsONIA OLIGOPHYLLA, / v. AZ. North-west interior (Stuart).

SWAINSONIA CANESCENS, / v7. JZ Somewhat less downy than the type
(F. v. M. in litteris), North side of Finke Gorge; margin of River Todd, north

side of Heavitree Gap |.

SwWAINSONIA cycLocarPa, 7. v. AZ. Near McDonnell Range (Schwartz).

SWAINSONIA UNIOFOLIOLATA, 2 v. AZ. At Kamarand’s Well, between George

Gill Range and Lake Amadeus (Spencer !). 20

154 HORN EXPEDITION—BOTANY.

SWAINSONIA MICROPHYLLA, 4. Gray. McDonnell Range (Schwartz) ; valley

of the Finke by Mount Sonder, and plain north of Ooraminna Pass !.

|| AlscHYNOMENE Inpica, Zezné. Banks of the Finke at Henbury! ; also by

Adminga Creek and waterholes of the River Stevenson !.

GLYCINE CLANDESTINA, Vend/and. Hermannsburg (Kempe); Blood’s Range
(Tietkens) ; Bagot’s Creek and ravines of Mount Tate !.

GLYCINE SERICEA, Bentham. Gill’s Creek (Tietkens); Glen Helen, and by
the Finke River near Mount Sonder !.

* KENNEDYA PROREPENS, /. v. JZ. Near (on!) Mount Sonder (Tietkens).
Extends to Barrow Range, W.A. (Elder Exped.),

* ERYTHRINA VESPERTILIO, Lentham. McDonnell Range and Mount Udor
(E. Giles) ; Krichauff Range (Kempe); Mount Sonder! (Tietkens) ; Finke Gorge

and Mount Francis !.

VIGNA LANCEOLATA, Bentham. Painta Spring and Glen Helen (Tietkens) ;
Alice Well at the Hugh River; also at Adminga Creek and by the River

Stevenson !.

|| Ruyncnosta MINIMA, De Cand. Stony places near Hermannsburg (Kempe) ;
Mount Sonder and Glen Helen (Tietkens) ; source of the Darwent River and by

Belt Range !.

|| Cassta Sopuera, Linné. River beds, Hermannsburg (Kempe); Mount
Sonder (Tietkens) ; Tempe Downs!.

Cassia vENuSTA, / v. MZ. Glen of Palms and McDonnell Range (E. Giles) ;
Tlpilla, Reedy Creek, Missionary Plain by Pine Point, by Belt Range and Stuart’s
Pass |.

CassIA NOTABILIS, /. v. J/. McDonnell Range (EK. Giles).

CasstA pLEUROCARPA, /. v. Mf. McDonnell Range (E. Giles) ; Glen Helen
(Tietkens) ; Hermannsburg (Kempe); R. Walker Gorge at Tempe Downs, Alice
Well, and extending to west and north on sandy flats by river channels ! ; Crown
Point !.

*Cassta GLuTiInosa, De Cand. Rocky tracts, Hermannsburg (Kempe) ;

Ipilla Gorge, Mount Francis, and Spencer Gorge off Stuart’s Pass !.

*CasstA pruINosA, / v. M. Rocky declivities at Penny Creek, in George
Gill Range, and of Mereenie bluff!

or

HORN EXPEDITION—BOTANY. le

CAssIA PHYLLODINEA, RX. Brown. River flats of the Upper Finke by Mount
Sonder, [pilla and Bagot’s Creek !.

CassIA EREMOPHILA, Cunn. Hermannsburg (Kempe); Mount Gillen !.

CassiA ARTEMISIOIDES, Gavd. Hermannsburg (Kempe); by Belt Range! ;
Alice Springs (F. J. Gillen !).

Cassta Sturru, 2. Browz. Tempe Downs, slopes of Mount Sonder and
5) ’ ]
Mount Francis !.

CasstA peso“ata, 7. 7. JZ. Hermannsburg (Kempe), Laura Vale (Tietkens);
by Belt Range, Horn Valley and Stuart’s Pass !.

PETALOSTYLIS LABICHOIDES, AX. Brown. Glen of Palms (bed of River Finke !)
(K. Giles); ranges, Hermannsburg (Kempe); Mount Sonder and Glen Helen
(Tietkens); Tempe Downs, Parke’s Gap, and between the Hugh River and

Engoordina |.
NEPTUNIA MONOSPERMA, 7. v. JZ. Near Hermannsburg (Kempe).

Acacia patens, /. v. JZ McDonnell Range (E. Giles), Mount Sonder
(Tietkens), Hermannsburg (Kempe); sand-plains, Laurie’s Creek to Glen Edith,
valley of Carmichael Creek, Missionary Plain towards Owen’s Spring, Ooraminna
Pass and towards James Range, thence to the Hugh River and Engoordina and

Crown Point !

ACACIA TETRAGONOPHYLLA, 72 v. JAZ. Hermannsburg (Kempe); Tempe

Downs, and sparsely distributed throughout the region !.

ACACIA SESSILICEPS, /. v. JZ. Hermannsburg (I<empe); base of Mount
Sonder, between Hermannsburg and Ellery Creek, Alice Creek, also Charlotte
Waters |.

* ACACIA LYCOPODIFOLIA, Cuzz. McDonnell Range (KE. Giles) ; rock surfaces,
Ilpilla Gorge, slopes of Mount Tate, on Mount Sonder, on Mount Francis, Horn
Valley, Stuart’s Pass !.

* ACACIA SPONDYLOPHYLLA, /. v. JZ. Glen of Palms and McDonnell Range
(E. Giles), Mount Sonder (‘Tietkens).
ACACIA MINUTIFOLIA, /. v. JZ. Hermannsburg (Kempe).

ACACIA ULICINA, JZerssner, var. oxyclada. West of McDonnell Range
(‘Tietkens).

204

156 HORN EXPEDI'TION—BOTANY.

Acacia Sentis, / v. JZ. Hermannsburg (Kempe); river flats by Mount

Sonder, and generally distributed !.

ACACIA FRUMENTACEA, Za/e, n. sp. Reedy Creek and by Mount Sonder ;

alluvial flats about Alice Creek and general thence south to Charlotte Waters !.

ACACIA NOTABILIS, / v. JZ. Mount Sonder and Gill’s Creek (Tietkens) ;
Carmichael Creek by Mereenie Bluff! ; Laurie’s Creek !.

Acacia sauicina, Lindley. McDonnell Range (E. Giles), Hermannsburg
(Kempe), Mount Sonder (Tietkens). Very general, on rich alluvial flats attaining
to 40ft. and d50ft. high !.

* ACACIA STRONGYLOPHYLLA, /. v. MZ. Rocky ground; Glen of Palms
(E. Giles), Palm Creek!, and Hermannsburg (Kempe) ; Mount Sonder! (Tietkens) ;

Mount Tate, Stuart’s Pass, and I]pilla Gorge !.

ACACIA PYRIFOLIA, De Cand. Gill’s Creek, Laura Vale, and Warman Rocks
(Tietkens) ; base of Mount Francis !.

ACACIA ESTROPHIOLATA, /. v. JZ. Hermaunsburg (Kempe).

ACACIA CORIACEA, De Cand. South McDonnell Range !.

ACACIA DICTYOPHLEBA, /. v. M. Hermannsburg (Kempe), north of Mount
Harris (Tietkens) ; Mounts Tate and Gillen!; near Gosse Range (Spencer).
Chiefly on sandhills, Idracowra, Henbury, Chambers Pillar, Engoordina to

Mount Squire and Crown Point. Var. with narrow oblong-lanceolate leaves

under one inch ; by Mount Francis !.
ACACIA LYSIPHLOIA, /% v. J. Hermannsburg (Kempe).
ACACIA stipuLIGERA, /. v. JZ. Near McDonnell Ranges (E. Giles).
ACACIA ACRADENIA, /. v. JZ. North of Mount Harris (Tietkens).

ACACIA CYPEROPHYLLA, & v. AZ. Warman Rocks (Tietkens), Mount Udor
(E. Giles), from description “ Geogr. Travels,” p. 32; also by margin of creeks
flowing on scarped face of Stanley Tableland to the Stevenson River, and on the
east slope on Red Mulga Creek !.

Acacia ANEURA, & v. VM. Throughout the region, forming dense scrubs and
ascending to high elevations; in rich soils attaining to 30ft. or 40ft. high !.

Hermannsburg (IXempe).

HORN EXPEDITION—BOTANY. tay

Acacia Krempwana, /& v. AZ. Finke River (Kempe); Laurie’s and
Carmichael Creeks !. Common in the valley of the Hugh, thence to Engoordina
and south to the Goyder River !.

Acacta Doravoxyton, Cun. Twelve miles south-east of Gills Creek
(Tietkens) ; also Mount Olga (Tietkens) and Ayers Rock (Spencer !).

* AcactA CowLEANA, Zafe, n. sp. Slopes of Mount Tate, near source of

Carmichael Creek, slopes of Mount Francis !.

)}AcaciA Farnestana, WWididenow. Chiefly in the channels of creeks,

Henbury, Tempe Downs, Rudall Creek, Goyder Pass, Upper Finke,- and tribu-

taries by Mount Sonder!; Hermmannsburg (kempe); Mount Sonder (‘Tietkens) ;

5

also Red Mulga Creek near Dalhousie Springs |.

CRASSULACEA.

| TILLBA VERTICILLARIS, De Cand. Henbury !, Conlin’s Lagoon !.

SALICARIEA.

RovraLA VERTICILLARIS, Ziznué. West of MeDonnell Range (Tietkens) ;

Carmichael Creek !.
ROTALA DIANDRA, / v. IW. Near McDonnell Range (Dittrich).
| AMMANNIA MULTIFLORA, Roxburgh. Mount Sonder (Tietkens).

| AMMANNIA AURICULATA, TV7d/dencw. Common by river margins, Mount
Sonder ! (Tietkens) ; Stuart’s Pass, Carmichael Creek, and south to Adminga Creek

and River Stevenson !.

| LyrHRUM HyssoPIPOLiA, Zizné. Margin of Conlin’s Lagoon !.

HALORAGEA.

Loupon1a AurEA, Lindley. Sand plain bordering George Gill Range and

around Glen Edith !.

Haboraais Gosser, / v. JZ. Glen ot Palms (E. Giles) and Hermannsburg
(Kempe) ; Alice Springs (C. Giles) ; Chambers Pillar !.

Haboracis oponrocarra, / v. JZ Mulga serub four miles north-east from
Glen Edith !.

_
>) |
Oo

HORN EXPEDITION

BOTANY.

Hatoracis AsPpeRA, Lindley. Hermannsburg (Kempe); slopes of Mount
Sonder ! (Tietkens) ; by Belt Range, Henbury !

MyriopHyLLuM veERRUCOSUM, Lindley. River Finke, near Hermannsburg
(Kempe), at Palm Creek, Running Water, and Henbury! ; Darwent River !.

MYRTACEEZ.

CALYCOTHRIX LONGIFLORA, / v. WM. McDonnell Range (KE. Giles); Her-
mannsburg (Kempe); north of Mount Harris (Tietkens); sandhills between
Bagot’s Creek and Winnall Range, and north-east from Glen Edith !.

THRYPTOMENE MAatsonguvul, /. v. J. River Finke (E. Giles); near Mount
Sonder, Glen Edith, and Gill’s Creek (Tietkens); sandhills chiefly between
Sullivan’s Creek and Idracowra ; Eagle Plain, Palmer River; between Laurie’s
Creek and Glen Edith, thence into the valley of Carmichael Creek ; between
Ooraminna Pass and James Range, thence to Hugh River and south to Crown

Point !; occasionally on rocky declivities, as at Tempe Downs, Bagot’s Creek, ete. !.

THRYPTOMENE FLAVIFLORA, 7. v. Wf. McDonnell Range (E. Giles) ; sand

country south side of George Gill Range, and between Laurie’s Creek and Glen
Edith !.

* BECKEA POLYSTEMONEA, / v. JW. Brinkley Bluff (Stuart); in McDonnell
Range (E. Giles) ; Mount Harris (Tietkens).

MELALEUCA PARVIFLORA, Zind/ey. Hermannsburg (Kempe).

MELALEUCA GLoMERATA, /. v. M. River Finke at Hermannsburg (Kempe) ;
river banks throughout the region !.

MELALEUCA, sp. <A tree forty feet high, bark papery, leaves cylindrical,

glaucous, and longer than J. g/omerata ; Spencer Gorge !.

Eucatyprus microrureca, / v. AZ. McDonnell Range (Stuart); flooded
ground by River Todd at Heavitree Gap; but abundant south of Charlotte
Waters.

* KUCALYPTUS PACHYPHYLLA, / v. MW. Glen of Palms (E. Giles) and Krichauff
Range (Kempe) ; gorge of Reedy Creek, ravine on south side of Mount Tate, on

Mount Sonder !.

Evucatyprus oLnosa, / v. MM. Hermannsburg (Kempe); Illamurta!; con-

stituting dense scrubs on the taluses of the ranges as about the sources of

HORN EXPEDITION—BOTANY, 159

Carmichael Creek, Glen Helen, Mount Sonder, Horn Valley, and south flank of
MeDonnell Range in the Valley of the Hugh !.

Evucatyprus Ouprienpu, /. v. J. Hermannsburg (Kempe); sandhills by
junction of Palmer and Walker, Missionary Plain by Pine Point, slopes of Mount

Francis !.

Var. with leaves oval-oblong to ovate-obcordate, one to one-and-a-quarter

inches long. Slopes of Mount Sonder !.

Eucatyprus TresseLuAris, /. 7. J. Hermannsburg (Kempe); sandy and
alluvial flats, Henbury, south side of George Gill Range, by Belt Range, by the
Lower Hugh River and elsewhere, extending south to Crown Point, the Goyder
and Charlotte Waters !.

Evcatyptus rostrata, Schlecht, River channels throughout the region! ;

’

Hermannsburg (Kempe).

Evcatyptus GAmopiyLLa, Fv. Jf. Hermannsbure (Kempe); Mount
Sonder (Tietkens) ; gregarious chiefly on sandy soil, as about junction of Finke
and Palmer Rivers, valley of the Walker; but also on stony taluses and rocky

declivities, as at Mount Tate, Belt Range and Mount Gillen !.
Evucatyptus serosa, Schauer. Laura Vale and Gill’s Creek (Tietkens),

* EUCALYPTUS TERMINALIS, /. 7. J. Hermannsburg (Kempe); widely dis-
tributed, chiefly on rocky declivities and tablelands, Tempe Downs to George Gill
Range, Mereenie Hscarpment to Mount Sonder and Stuart’s Pass, Mount Gillen

to James Range !.

Kucatyprus EupEsMorpEs, #7. J/. Sandhills between Bagot’s Creek and

Lake Amadeus (Spencer !).

RHAMNACEA.

VENTILAGO VIMINALIS, /Zookev, Hermannsburg (Kempe); Goyder Pass and
Burt Plain !.
* CRYPTANDRA SPATHULATA, 4. v, JZ. Glen of Palms (K. Giles) and Krichauff

Range (Kempe) ; Laurie’s Creek !.

UMBELLIFERA.

* HyprocoryLe TrRacHycarPA, 7. v. J. Near Hermannsburg (Kempe) ;

shaded rocks, Bagot’s Creek, Mount Tate, Horn Valley and Finke Gorge !.

160 HORN EXPEDITION—BOTANY.

* Dipiscus GILLENmH, Za/e, n. sp. On Mount Gillen near Alice Springs !.

Dipiscus Guiauctrouius, / v. JZ River Finke (Stuart); Hermannsburg
(Kempe): Glens Helen and Edith (Tietkens); not infrequent in alluvial soil,

George Gill Range, Chambers Pillar, ete. !
* Actinotus Scuwartzil, 7 v. 47. On Mount Sonder (Schwartz).

|| Daucus BRacutatus, Sveber. Hermannsburg (Kempe); margins of creeks,
Henbury, Glen Helen, Upper Finke by Mount Sonder !.

SANTALACEEA.

Exocarpos spartEA, 2. Lrown. Ranges and sandhills about Hermannsburg
(Kempe); sand plain off Bagot’s Creek, between Glen Edith and Carmichael

Creek, and valley of Upper Finke by Mount Sonder !.

* ANTHOBOLUS EXOCARPOIDES, / v. M7. McDonnell Range (E. Giles), on
rocky slopes of Mount Tate !; extends to Cavenagh Range (Elder Exped.).

SANTALUM LANCEOLATUM, 2. Brown. Hermannsburg (Kempe), Henbury and

THamurta !.

SANTALUM ACUMINATUM, A. de Cand. McDonnell Range (EK. Giles), Her-
mannsburg (Kempe). Of frequent occurrence in the alluvial bottoms of the river
gorges and alluvial flats of valleys, such as at George Gill Range and the

Upper Finke |.
LORANTHACEE€Z.

Lorantnus Exocarpt, Behr. Hermannsburg (Kempe), near Mount Sonder

(Tietkens) Widely dispersed throughout the region !.

LORANTHUS LINOPHYLLUS, /e7z/. Hermannsburg (Kempe). Widely dis-

persed !.

LORANTHUS GIBBERULUS, Zaze. Glen Helen (Tietkens) ; on Grevillea striata
at Mount Francis, Goyder Pass, Burt Plain, and by River Todd at Alice Springs ! ;
on Grevillea agrifolia at Palm Creek!; on Hakea leucoptera, between James
Range and Alice Creek !.

LoraNtHUS PENDULUS, Sreber. Hermannsburg (Kempe), Glen Edith (Tiet-
kens) ; Stuart’s Pass !.

Lorantnus Quanpanc, Lindley. Hermannsburg (Kempe). Ranging with

its chief host-plant, Acacia aneura !.

HORN EXPEDITION—BOTANY. 161

PROTEACEA.

GREVILLEA PTEROSPERMA, /. v7. JZ. A wide-spreading tree of about twenty

feet high ; sand-plain off Bagot’s Creek !.
GREVILLEA STENOBOTRYA, /. v. AZ. McDonnell Range (E. Giles).

GREVILLEA ERIosTAcHYA, Lindley. Glen Edith (Tietkens), as G. chryso-
dendron ; sand-plain between Glen Edith and Carmichael Creek !.

GREVILLEA JUNCIFOLIA, //ooker. MeDounell Range and Glen of Palms
(E. Giles), ranges by Hermannsburg (Kempe), Engoordina (Tietkens) ; Chambers

Pillar, lara Water, and by junction of Palmer and Walker Rivers !.
GREVILLEA ANGULATA, 2. Brown. HWermannsburg (Kempe).

GREVILLEA Wickitami, JZerssver. Glen of Palms, Gosse’s Range, and
MeDonnell Range (E. Giles).

*GREVILLEA AGRIFOLIA, Cunv. McDonnell Range (Stuart), Glens Edith and
Farewell (Tietkens). Rocky ravines and declivities, Ipilla, Reedy and Penny’s
Creeks, Mount Tate, Mount Francis, Mount Sonder, Stuart’s Pass, Mount Gillen
and Palin Creek !.

GREVILLEA stRIATA, 2. Browz. Sand-flats near Idracowra, Henbury, south
side of George Gill Range, by Belt Range, valley of the Upper Finke, Goyder
Pass, Burt Plain, valley of the Todd River near Alice Springs !; Hermannsbure
(Kempe).

GREVILLEA NEMATOPHYLLA, / v7. JZ. Sandhills and plains, Chambers Pillar,
south side of George Gill Range, between James Range and River Hugh, thence

to Engoordina, Crown Point and Charlotte Waters !.

Hakera Lorna, 2. Brown. Glen of Palms and McDonnell Range (E. Giles).
Sandy or loamy soil, not infrequent, as at Henbury and Carmichael Valley! ;
more common about Crown Point, in the valley of the Goyder, thence to Charlotte
Waters !.

Hakra purpurea, S/fooker. Between Lakes Amadeus and Macdonald
(Tietkens).

Hakra Leucoprera, R. Brown. Loam flats and sandhills, widely distributed

throughout the Larapintine region! ; Hermannsburg (Isempe).
21

162 HORN EXPEDITION—BOTANY.

HAKEA MULTILINEATA, JZezssnexr. On Mount Sonder! (Schwartz); also on
Bogey Flat between Goyder River and Mount Daniel; north side of Crown

Point !.

RUBIACEA.

OLDENLANDIA GALIOIDES, /. v. JZ. West of McDonnell Range (Tietkens).
OLDENLANDIA TILLHACEA, / v. AZ. Carmichael Creek and Mount Francis !.

CANTHIUM LATIFOLIUM, /. v. AZ. Central Australia (Stuart); McDonnell
Range (E. Giles); stony ground chiefly in the ranges, near Hermannsburg
(Kempe) ; between Running Waters and Ilpilla, south side of George Gill Range,

Glen Helen, and elsewhere !. Extends south to Arkaringa Valley (Elder Exped.).

PoMAX UMBELLATA, So/ander. McDonnell Range (E Giles); Hermannsburg
(Kempe) Sandhills at Idracowra, rock surface at Tempe Downs, and in Bagot’s
Creek Gorge !.

CUCURBITACEA.

|| Cucumis Crater, Zinné. McDonnell Range (E. Giles); Hermannsburg
(Kempe); south side of George Gill Range, Stuart’s Pass!; also by River

Stevenson and at Gidia Creek near Oodnadatta !.

| MeLoruria MaAprErRASPATANA, Cognx. Hermannsburg (Kempe); near
Mount Sonder, Engoordina (Tietkens). Common in bushy places, Stuart’s Pass,

Horn Valley !, ete.

COMPOSITA.

BRACHYCOME CILIARIS, Zesstzg. Running Water!, Mount Francis !, Conlin’s
Lagoon |}.

*Var. glandulosa. Branches lax, spreading two and three feet, flowers
blue or white, leaves varying from pinnate to linear-lanceolate, with long linear
serratures. Saxatile at Tempe Downs, Reedy Creek, Glen Helen Gorge and

Palm Creek !.

MinurRIA LEPTOPHYLLA, De Cand. McDonnell Range (C. Giles); IIpilla,
slopes of Mereenie Bluff, sand-plain north-east of Glen Edith, and between the
Todd and Ooraminna Pass!; Alice Springs (F. J. Gillen !),

HORN EXPEDITION—BOTANY. 163

Minurta Cunnincuamu, Lertham. UWermannsburg (Kempe); Idracowra,

junction of Palmer and Finke Rivers, Stokes Pass !.

CALoris DENTEX, R. Brown. Mallee scrub, a few miles north-east from Glen
Edith !.

CaALoris CYMBACANTHA, /. v. AZ, Ooraminna Pass!; also at the Goyder River !.

CALOvIS ERINACEA, Sfeefs. Sub-shrubby, spreading hemispherically to about
three feet diameter. Sandhills at Idracowra, Reedy Creck, River Hugh at Alice
Well, thence south to Crown Point, the Goyder and Stevenson Rivers |.

CALOTIS LAPPULACEA, Bentham. Sandy ground, Hermannsburg (Kempe) ;
Carmichael Creek !.

CALOTIS MICROCEPHALA, Bentham. Hermannsburg (Ikempe).

CaLotis LatiuscuLa, /. v. AZ. and Zate. Near Finke River (éeste F. v. M.) ;

Sullivan’s Creek, south side of George Gill Range and Glen of Palms}.

CaALoTis PLUMULIFERA, /. v. AZ, Carmichael Creek (with several rows of ray-
florets) ; Glen Helen !

CALoris porPHyROGLOssA, / v. JZ, Conlin’s Lagoon, near Alice Springs ;
also by the River Stevenson !.

CaLotis HIsprpULA, / v. JZ. Hermannsburg (Kempe); east end of George

Gill Range, Carmichael Creek, Finke River by Mount Sonder !.

Catotis Kemper, “. v. J. Perennial, spreading to about two feet high,

Hermannsburg (Kempe), Engoordina, and also abundant at the Goyder River !
t= | ’ oD >

AstER Mitcuenui, / v. iW. McDonnell Range (KE. Giles), Hermannsburg
(Kempe).

* Aster Ferresu, 2 v. Jf. Brinkley Bluff (Stuart), McDonnell Range
(E. Giles), Krichautf Range (Kempe); Bagot’s Creek, Belt Range, and Stuart’s

Pass !.

* ASTER MEGALODONTUS, /. v. JW. Flowers blue. Chandler Range, Ipilla
Gorge, Tempe Downs, George Gill Range, Mount Sonder, Goyder Pass, Iinke

Gorge, Stuart Pass, Mount Gillen, Ooraminna Pass !.

VITTADINIA AUSTRALIS, . Richard. Sandy soil, Hermannsburg (lkempe) ;
Tempe Downs (with 3-lobed leaves), south side of George Gill Range, Upper

Finke by Mount Sonder !

214

164 HORN EXPEDITION—BOTANY.

* VITTADINIA SCABRA, De Cand. Ilpilla Gorge, Tempe Downs, Darwent
River Gorge, Finke Gorge !.

PopocoMA CUNEIFOLIA, #. Lrown. McDonnell Range (C. Giles); Mount
Sonder (Tietkens) ; near Hermannsburg (Kempe); on limestone rubble east of
reorge Gill Range and by Mereenie Bluff; Engoordina (occasionally with white
flowers) !.

PLUCHEA TETRANTHERA, / v. JZ. Hermannsburg (Kempe).

Prucuea Eyrea, / v. M. McDonnell Range (EK. Giles); Hermannsburg
(Kempe); usually on marshy ground, Ilamurta, Bagot’s Creek, ravine of Mount
Tate, Redbank Gorge, Finke Gorge, Stuart’s Pass, Painta Spring !.

* PLUCHEA squarRRosA, Bentham. Bagot Creek in George Gill Range, Palm
Creek in Krichauff Range, Redbank Gorge, Glen Helen!.

PTERIGERON LIATROIDES, Lentham. Laura Vale (Tietkens); Henbury and
Ilpilla Gorge !.

PreRIGERON MICROGLOSSUS, Bentham. Sandy tracts, Hermannsburg (Kempe).

PrERIGERON DENTATIFOLIUS, / v. J. Between McDonnell Range and
Charlotte Waters (C. Giles).

|| EPALTES AUSTRALIS, Lessing. Reedy Creek in George Gill Range!; also
Crown Point and River Stevenson }.

*PrerocauLon Biniarpiert, & v. JZ Hermannsburg (Kempe); Belt
Range, Horn Valley, Finke Gorge, and on Mount Gillen !.

PreRocAULON SPHACELATUS, Lentham. McDonnell Range (Stuart); also
Crown Point !.

|| GNAPHALIUM LUTEO-ALBUM, Ziznzé. Common throughout the region!; Her-
mannsburg (Kempe), Painta Spring (Tietkens).

|| GNAPHALIUM JAPonicuM, Zhunderg. Finke Gorge |}.

| GNAPHALIUM Inpicum, Zizné. Hermannsburg (Kempe).

IXI0OLENA TOMENTOSA, Sonder and /. v. M. Hermannsburg (Kempe) ; sand-
hills, Tempe Downs, Darwent River, Alice Creek, and Lower Hugh River !.

PODOLEPIS CANESCENS, Cun. Sandhills, Hermannsburg (Kempe) ; Ooram-
inna Pass and between there and James Range !.

Popoteris Siemssenu, “2 v. JZ. Stuart’s Pass by Brinkley Blulf!.

WairziA coryMBosa, /Vendland. Ooraminna Pass !.

HORN EXPEDITION— BOWVANY. 165

HeniprerumM FLoRIBUNDUM, De Cand. Hermannsburg (Kempe) ; junction of
Finke and Palmer Rivers, Carmichael Creek ! ; Alice Springs (I. J. Gillen !).

HenrprerumM sriprratum, & v. JZ River Finke (Stuart), McDonnell Range

(E. Giles); sandhills, Hermannsburg (Kempe), Running Water, T!pilla, and

between Ooraminna and James Ranges !. Extends to Barrow Range and Victoria
fo) fo)

Desert (Elder Exped.).

Hewiprerum iINcANUM, Ve Cand. Stony ground, Hermannsburg (Kempe) ;

Tpilla Gorge and Mount Sonder !.

Heviprerum Frrzcipsont, #7. JZ Hermannsburg (Kempe), Tempe Downs
(Thornton), Mount Squire !; also west of Eringa (Tietkens). Extends to Barrow
Range and Victoria Desert (Elder Exped.).

HeLIPrERUM HYALOSPERMUM, / v. AZ. Finke Gorge !.
HeLiprerum stricrum, Lertham. Stuart’s Pass by Brinkley Bluff !.

Hentprerum Cuarstry®, # v. JZ Hermannsburg (Kempe); clay flats and
flooded ground, sources of Laurie’s and Rudall’s Creeks, Carmichael Creek,
Darwent River, Glen Helen, Upper Finke by Mount Sonder, Conlin’s Lagoon,
and valley of the Upper Hugh River! ; also by the River Stevenson !,

Hewviprerum moscuatum, Bertham. Hermannsburg (Kempe), Engoordina !.

HewipreruM Tierkensi, & v. JZ Hermannsburg (Kempe); Darwent River,
Glen Edith, and Horn Valley !.

HELIPTERUM PrEROCHEHTUM, Lertham. Hermannsburg (Kempe) ; Bagot’s

Creek, by Mount Francis, Glen Helen, and Mount Squire !.

Henicurysum Ayersu, / v. JZ Limestone rubble, east end of G. Gill
Range, Hope Valley !, Ooraminna Pass !, Alice Springs (C. Giles), Finke River
(Kempe); also Mount Olga (Gosse), Everard Range, S.A., and near Mount Squires,
Cavenagh Range, W.A. (Elder Exped.). [The specimens obtained by the Horn
Expedition are somewhat aberrant as regards the pappus of the exterior flowers,
which is more rigid, with the bristlets connate towards the base into bundles, the
numbers in the sets varying from few to several. The plant reaches the height of

1}ft. It reminds in some respects of Ixioleena and Podolepis.—F. v. M.}.

Hericurysum Cassintranum, Gaud. River Finke (Stuart), McDonnell Range

(EK. Giles), Hermannsburg (Kempe) ; sandy ground, Hpilla and Ooraminna Pass !.

166 HORN EXPEDITION—BOTANY.

Heticurysum LAwreNceLLA, 7. v. JZ. Shady and moist places, Hermanns-
burg (Kempe) ; Ooraminna Pass !.

HeticurysumM Luctpum, Afenckel. Glen of Palms (EK. Giles) ; Missionary

Plain ! and Hermannsburg (Kempe); Chamber’s Pillar and Reedy Creek !.

* HELICHRYSUM AMBIGUUM, Zurvcz. Young foliage viscid; rocky ground at
Llpilla Gorge, Mount Francis, Finke Gorge, Palm Creek and Mount Gillen !.

VAR. semicalvum. McDonnell Range (Stuart) ; sandhills, Idracowra, also
5 ) ) 5)
Crown Point and River Stevenson !.

HeLicurysum apicuLtatum, Zurcz. Throughout the region on sandy soil!.
Hermannsburg (Kempe).

* Heticurysum Tuomsont, / v. AZ. McDonnell Range (E. Giles); shaded
rocks, Krichauff Range (Kempe), Tempe Downs, Bagot’s Creek Gorge, Redbank
Gorge, Stuart’s Pass, and Simpson’s Gap near Alice Springs. Before expansion of
the inflorescence the subwoody stem is about six inches high. Extends to Mount

Olga (E. Giles).

* HeLicurysuM Kempel, /. v. AZ. Crevices of rock-faces, Krichauff Range
(Kempe), Brinkley Bluff and Heavitree Gap !.

RurTiIposis HELICHRYSOIDES, De Cand. Hermannsburg (Kempe); sandy soil,
south side of G. Gill Range, valley of the Darwent River and Lower Hugh River !.

MitiotiA Kemprt, / v. WZ. Sandhills, Hermannsburg (Kempe).

MyriocepHaLus Sruartu, Bentham. Wermannsburg (Kempe) ; Carmichael
Creek !.

ANGIANTHUS PUSILLUS, Bentham. Bagot’s Creek Gorge !.

GNEPHOSIS CYATHOPAPPA, entham. Burt Plain and plain north of Oora-
minna Range !.

EriuocutaAmys Kwnappu, 4. v. JZ Hermannsburg (Kempe).

CALOCEPHALUS PLATYCEPHALUS, Lenxtham. McDonnell Range (E. Giles) ;
Henbury, Darwent River Valley, Glen Helen, Upper Finke Valley near Mount

Sonder !; also at the Goyder River !

|| SIEGESBECKIA ORIENTALIS, Linné. Hermannsburg (Kempe), Stokes Pass,
Finke Gorge and Stuart’s Pass !.

HORN EXPEDITION—BOTANY, 167
WEDELIA VERBESINOIDES, 7: 7. JZ Finke River (Stuart).

* WEDELIA STIRLINGH, Za/e, n. sp. Rocky and stony ground, Stokes Pass,
slopes of Mereenie Bluff, Mount Francis and Mount Sonder, Finke Gorge and
Stuart’s Pass !.

| Brpens siprnnatus, Zinvé. Hermannsburg (Kempe), Mount Sonder
(Tietkens).

| GLOSSOGYNE TENUIFOLIA, Cassin7. Hermannsburg (Kempe), Mount Sonder
(Tietkens); River Finke between Henbury and Parke’s Gap, Glen Helen, Stuart’s
Pass !; Alice Springs (F. J. Gillen !).

|| CENTIPEDA ORBICULARIS, Louvetvo. Mount Sonder (Tietkens); by the Finke

River at Henbury and by Mount Sonder !.

CENTIPEDA THESPIDIOIDES, /. v7. Jf, Finke River (Stuart), by Mount

Sonder !.

Senecio Grecoru, “ v. AZ, Finke River (Stuart), McDonnell Range (EF.
Giles), Mount Sonder (Tietkens), Hermannsburg (Kempe), Carmichael Creek,

and not uncommon throughout the region !.

Senecio MAGNIFICUS, 72 7. JZ. Hermannsburg (Kempe), Carmichael Creek,

Horn Valley, and generally on rich alluvial flats !.

-SeNecto Lautus, Solander. Wlamurta, Tempe Downs, and banks of Upper

Finke by Mount Sonder !.

SENEcCIO oporaAtus, Hornemann. Hermannsburg (Kempe), also sandhills

by River Stevenson !.

Senecio Cunnincuamil, De Card. By junction of Palmer and Finke Rivers '.

HRECHTITES PICRIDIOIDES, Zircs. Moist sand of river beds, by Hermanns-

burg (Kempe).

ERECHTITES LACERATA, /. v. AZ. Glen Farewell (Tietkens) ; by moist river
banks as at Bagot’s and Reedy Creeks, Upper Finke by Mount Sonder, Alice

Springs |.

The occurrence of SoNcHUS ARVENSIS along the Finke towards its source was
noted by E. Giles as early as 1872: it may have originated from the visits of
Stuart in 1860-1862, if so it has spread since then, as it was observed very

frequently along that river from Crown Point to Mount Sonder.

168 HORN EXPEDITION—BOTANY.

CAMPANULACEA.

*TsoromMaA peTRmA, /. v. AZ. James Range and Hugh River (Stuart),
McDonnell Range (E. Giles), Hermannsburg (Kempe), Glen Edith (Tietkens) ;
shaded rocks, Tempe Downs, George Gill Range, Mount Tate, Finke Gorge,
Stuart’s Pass, Alice Springs !.

| WAHLENBERGIA GRACILIS, A. de Cand. Hermannsburg (Kempe) ; widely
distributed, plains and valleys !.

CANDOLLEACEZA.

CANDOLLEA FLORIBUNDA, /. v. MZ. McDonnell Range (E. Giles), loam flat
by Conlin’s Lagoon near Alice Springs !.

GOODENIACEEA.

BRUNONIA AUSTRALIS, Sy7th. McDonnell Range (E. Giles); sandy ground,
Hermannsburg (Kempe), Running Water, Chambers Pillar, and between Oora-

minna and James Ranges!; Alice Springs (I. J. Gillen !).

LESCHENAULTIA DIVARICATA, /. v. MZ. Wide spread, Hermannsburg (Kempe).
Sandhills by the Lower Hugh and south to Charlotte Waters !.

CatosPperMA Mvue.iert, Bentham. Near McDonnell Range (Dittrich). Sand
plain stretching from south-west slope of Mount Tate!. Extending south to
between the Alberga and Mount Olga (E. Giles).

SCHVOLA SPINESCENS, 2. Brown. Off Penny’s Creek in George Gill Range.
Common from Engoordina to Charlotte Waters !.

Sc#voLta PARVIFOLIA, 7. v. AZ. Alice Springs (C. Giles), Hermannsburg

(Kempe) ; Idracowra, Illamurta and Mereenie Bluff!.

SCHVOLA DEPAUPERATA, 2. Brown. McDonnell Range (EK. Giles), Hermanns-
burg (Kempe). Sandhills and plains, Idracowra, Chambers Pillar, Laurie’s Creek,
between Glen Edith and Carmichael Creek, valley of the Lower Hugh River and
thence to Charlotte Waters !.

*ScHVOLA OVALIFOLIA, 2. Brown. Glen of Palms (EK. Giles), Alice Springs
(C. Giles), slopes of and on! Mount Sonder (Tietkens); rocky ground at Mount

Francis and in Stuart’s Pass !.

HORN EXPEDITION—BOTANY. 169

* GooprmntA Rameti, /. v. AZ. Stony or rocky ground, Krichauth Range

y) Jyo5 5

Kempe 3agot’s Greek Gorge, Mount Tate, Mount Francis, Glen Helen
2 : + eet | ’ , ’

Mount Sonder and Mount Gillen !.
GoopENIA nirsutA, /) v. AZ Central Australia (Stuart).

*GoopENnIA Vin~MorInI&, /2 v. AZ Hermannsburg (Kempe). Stony ground,

Mereenie Bluff and Mount Francis !.

Goopenta Nicnoxsont, “2 v. JZ North-west interior (Stuart).
GOODENIA GRANDIFLORA, S7vis. Dashwood Creek (Tietkens).

“GoopentA Horntana, Jaze, n.sp. Growing in rock crevices, south escarpe-

ment of George Gill Range at Ready and Penny’s Creek, Stuart’s Pass!
GoopDENIA StrRaANGFORDH, 7. v. JZ Hermannsburg (Kempe).

GoopentA Mueckrana, / v. JZ Between Mount Udor and George Gill

Range (E. Giles) ; sandhills, Hermannsburg (Kempe) ; Tempe Downs (Thornton).

GoopENIA LARAPINTA, Za/e, n. sp. Reedy Creek, sand plain north-east of
Glen Edith, slope of Mereenie Bluff, and at Glen Helen !

GooDENIA HETEROCHILA, /. 7. JZ. Alice Springs, softly hirsute, and Eagle

Plain, a narrow-leaved variety !.

GoopentA MircuEeniy, Bextham. Alice Springs and Charlotte Waters (C.
Giles).

GOODENIA SEPALOSA, /. 7. JZ, Hermannsburg (Kempe)

GoopENnta cycLoprera, KR. row. Hermannsburg (Kempe); Gosse Range
(J. Schmidt). Sandy ground by Running Waters, thence extending south to River

Stevenson, ete. !.

GoopENIA suBINTEGRA, /. 7. AZ Finke River (R. Warburton) ; Gosse
Range (Schwartz); Running Waters!; Alice Springs (F. J. Gillen !); also Charlotte
Waters (C. Giles).

GoopENIA Microprera. /. v. AZ Alice Springs and Charlotte Waters (C.
Giles).

VeLueya connata, 7. v. AZ McDonnell Range (E. Giles); Hermannsbure
(Kempe); Laura Vale and Warman Rocks (Tietkens); Alice Springs (F. J.

Gillen !). 22

170 HORN EXPEDITION—BOTANY.
GENTIANEA.

| EryrHre®a spicata, Persoon. McDonnell Range (E. Giles) ; sand of river-
beds, Hermannsburg (Kempe) ; Conlin’s Lagoon near Alice Springs !.

PLANTAGINEA.

Prantaco varia, 2. Brown. Upper Finke by Mount Sonder and Ooraminna

Pass !

PRIMULACEZ.

|| SAMOLUS REPENS, Persoon. Hermannsburg (Kempe); Iamurta Soakage ;
River Walker at Tempe Downs; River Finke at Finke Gorge, and Palm Creek !.

JASMINEZ.

JASMINUM LINEARE, &. Brown. McDonnell and Gosse Ranges (KE. Giles);
Hermannsburg (Kempe) ; Bond Spring and Mount Sonder (Tietkens). South side

of George Gill Range !.

JASMINUM CALCAREUM, /. v. AZ. McDonnell Range (E. Giles); Krichauff
Range (Kempe), Mount Sonder (Tietkens) ; Tempe Downs, edge of plain on south
side of George Gill Range, by the Upper Finke and at Stuart’s Pass !,

APOCYNEA.

Carissa Brown, /. v. JZ, var. lanceolata. Glen of Palms (Kempe). In
rocky channel of River Darwent, Mount Francis, Glen Helen, Horn Valley and
Burt Plain !.

ASCLEPIADEA.
CyNANCHUM FLORIBUNDUM, &. Lrown. Beds of creeks, Hermannsburg

(Kempe), Emily Gap, Glen Helen and Watson Hills (Tietkens); Upper Finke
and tributaries by Mount Sonder!; also at Crown Point and Goyder River!.

SARCOSTEMMA AUSTRALE, R. Lrown. Hermannsburg (Kempe) ; Bagot’s Creek
Gorge, by the Hugh, on north side of Brinkley Bluff and at Painta Spring !.

DamuiaA Kemprana, /% v. JZ. Hermannsburg (Kempe); Mount Sonder,
Laura Vale and Warman Rocks (Tietkens); sand plain off Bagot’s Creek !.
Extends to Fraser Range, West Australia (Elder Exped.).

HORN EXPEDITION—BOTANY. LiL

MarspeniA LrICHHARDTIANA, /. v. JZ McDonnell Range (E. Giles),
Hermannsburg (Kempe), Mereenie Bluff (Tietkens), Burt Plain !.

CONVOLVULACEA.

Ipoma@a Murer, Bentham. McDonnell Range (EK. Giles), Bond Spring,
Mount Sonder! and Glen Helen! (Tietkens) ; Bagot’s Creek, Reedy Creek Gorge,
between River Todd and Ooraminna, at Deep Well in James Range!. Also

abundant by waterholes from Engoordina to River Stevenson !.

TpoMa@A RACEMIGERA, 7. v. AZ. and Zate. Glen Helen (Tietkens) Sandy
channel of the River Hugh in Stuart’s Pass !. Fruit, hitherto unknown, slightly
exceeding calyx, ovoid conic in vertical outline, roundly quadrangular in transverse
outline, longitudinally fine-striated, splitting into four valves, two-celled, one seed

in the whole capsule, seed clothed with short appressed hairs.

CoNVOLVULUS ERUBESCENS, Svs. McDonnell Range (E. Giles), Hermanns-
burg (Kempe) ; wide spread over the low level tracts !.

POLYMERIA LONGIFOLIA, Lizd/ey. Hermannsburg (Kempe).

PotymMeriA anacusta, Lindley. Hermannsburg (Kempe).

Breweria ROSEA, / 7. AZ. McDonnell Range and Glen of Palms (E. Giles),
Hermannsburg (Kempe).

| Evotvuius Linirouius, Lzxné. Brinkley Bluff (Stuart), McDonnell Range
(E. Giles), Krichauff Range (Kempe), Glen Helen (Tietkens), Alice Springs,
Ilpilla, sand plain off Bagot’s Creek, alluvial flats on Carmichael Creek,
Mereenie Bluff !.

| Cuscura ausrrRaALis, AR. Brown. Hermannsburg (Kempe). On young

plants of Cassta phyllodinea at the Walker and Palmer Rivers junction! ; Alice
Springs (F. J. Gillen !), on Boerhaavia diffusa. Also Charlotte Waters (C. Giles).

SOLANACEA.

SoLtanuM FeEROcISssIMUM, Zixaley. McDonnell Range (EK. Giles); Hermanns-
burg (Kempe) ; Bond Spring and Laura Vale (Tietkens) ; Glen Helen !.

*SoLANUM ORBICULATUM, Dunal. Mount Sonder (Tietkens).
SOLANUM ESURIALE, Lindley. McDonnell Range (KE. Giles). Sandy soil

Hermannsburg (Kempe); south side of George Gill Range, Tlara Water and Glen
fo} , Do o™,
Helen |. SH

A

eh HORN EXPEDITION—BOTANY.

Sovanum SrurtiAnum, / v. JZ Rocks near Hermannsburg (Kempe) and
Tempe Downs !.

SOLANUM EREMOPHILUM, / v, AZ. Reedy Creek Gorge; slopes of Mount Sonder !.

*SoLANUM PETROPHILUM, /. v. Jf. Bagot’s Creek Gorge, Stuart’s Pass and
on Mount Gillen !.

SoLANUM ELLIPTIcuM, &. Brown. On rich clay soil, also in the ranges, Finke
River (Kempe); Mount Sonder! (Tietkens). Rocks at Tempe Downs, [IIpilla
Gorge, Mount Tate, Mereenie Bluff, Mount Francis and Mount Sonder !.

Datura Leicuuarptu, / v. JZ By margins of all creeks, particularly the
Upper Finke and its tributaries!; Glen of Palms (KE. Giles) and Hermannsburg
(Kempe) ; Mount Sonder! (Tietkens).

NICOTIANA SUAVEOLENS, Zehmann. By margins of nearly all creeks from
south of Charlotte Waters to the Upper Finke!; Glen of Palms (E. Giles) and
‘Hermannsburg (Kempe).

Dusoista Hopwoopi, / v. 17. Near Mount Liebig (E. Giles), Hermanns-

burg (Kempe), Glen Edith (Tietkens). I]pilla and sand plain north-east from
Glen Edith!; on sand-hills between George Gill Range and Ayers Rock (Spencer!).

SCROPHULARINA.

|| Mimutus Gracizis, 2. Brown. Carmichael Creek !.

|Sremopia viscosa, Roxburgh. Mount Sonder! (Tietkens). By river
channels and water courses, between Engoordina and Sullivan’s Creek, at the
Finke-Palmer Junction, Tempe Downs, by Belt Range, Glen Helen, Stuart’s Pass,
Alice Springs, Lower Hugh River, and south to Lilla Creek and Goyder River !.

Sremopia Moreania, /& v. AZ. Hermannsburg (Kempe). Also Var. parvi-
tora, at the River Finke by Mount Humphries and at the Goyder River !.

| LimosELLA Aquatica, Zinné. Bagot’s and Laurie’s Creeks, Upper Finke
and tributaries by Mount Sonder, Stuart’s Pass and Conlin’s Lagoon !.

* BUECHNERA LINEARIS, 2. Brown. Near Mount Sonder (Tietkens) ; bed of
south ravine of Mount Tate !.

ExacHoLtoma Horn, & v. MZ. and Tate (gen. et spec. nov.).* Wet clay-

banks, Carmichael Creek at its junction with Deering Creek !.

* The authors regret that they cannot honour the patron of the Expedition as they would have wished,
because the generic name Hornia is already preoccupied in botanical nomenclature.

HORN EXPEDITION—BOTANY. 173

BIGNONIACEA.

*“TEcoMA ausrRALis, R. Brown. MeDonneli Range (Stuart) ; Mount Sonder
and Gill's Creek (Tietkens), Growing on rocky declivities, Krichauff Range
(Kempe), Tempe Downs, Ipilla Gorge, gorges of George Gill Range, Mount Tate,
Redbank Gorge and Stuart’s Pass. Extends to Everard and Barrow Ranges

(Elder Exped.).
ACANTHACEEA.

* RUELLIA PRIMULACEA, /. v. JZ. McDonnell Range (EK. Giles), Alice Springs
(C. Giles). On rocks at Parke’s Gap, Tlamurta and Horn Vailey !.

| JUSTICIA PROCUMBENS, Linné. Hermannsburg (Kempe) ; Mount Sonder and

Ooraminna (Tietkens). Common in the low level tracts !.

*Jusricia _Kemprana, / v. AZ. A dense shrub spreading from two to three
teet diameter; leaves cuneate-oval, dentate on the margin; flowers pink ; exclu-
sively confined to stony ground or rock-slopes. Hermannsburg (Kempe), Ipilla
Gorge, Horn Valley, declivities between Harris Creek and River Hugh, Oora-

minna Pass !.
LABIATA.

* PLECTRANTHUS PARVIFLORUS, 7ZenckedZ. Mount Sonder (Tietkens). Shaded
rocks, Hlara Water, Reedy Creek and Palm Creek !. Extends to Everard Range
(Elder Exped.).

* PROSTANTHERA SCHULTZ, 7. v. JZ, m.s., Cens., p. 169 (1889). “Ditters from
P. rotundifolia, R. Br., in smaller, less crenate and thicker leaves,” /. v. JZ. in

litteris. Flowers and fruit remain unknown. Higher slopes of Mount Sonder !.

* PROSTANTHERA WILKIBEANA, /. v. JZ. “Sandstone Rocks” and Mount
Sonder ! (Tietkens). Rocky declivities, Tempe Downs and George Gill Range !.
Extends to Everard Range (Elder Exped.), and between Mount Olga and Barrow

tange (E, Giles).

PROSTANTHERA Baxtert, Cuan. Shady places in Krichauff Range (Kempe) ;

Running Water }.

PROSTANTHERA STRIATIFLORA, /. v. JZ. Gosse and McDonnell Ranges
(E. Giles), Mount Sonder!, and Glen Edith (Tietkens). Rich plains, Hermanns-
burg (Kempe), Running Water, east end of George Gill Range, Bagot’s Creek

Gorge, by Belt Range, Alice Springs !.

174 HORN EXPEDITION—BOTANY.

TrevucRIUM RACEMOSUM, &. Brown. Mount Sonder (Tietkens), Finke River
(E. Giles).

TEUCRIUM GRANDIUSCULUM, /&% v. JZ. and Jaze. Watson Hills and Gill’s
Creek (Tietkens).

VERBENACEZ.

SPARTOTHAMNUS TEUCRIFLORUS, /. v. AZ. Hermannsburg (Kempe) ; Bond
Spring and Glen Helen (Tietkens). In shade of trees, south side of George Gill

Range !.

*SPARTOTHAMNUS PUBERULUS, / v. JZ. Base of escarpment at Heavitree
Gap! Foliage and stem stellately downy; leaves lanceolate, attenuate at the
base but sessile ; flowers not seen, fruit coral red.

VERBENA MACROSTACHYA, / v. JZ. Beds of creeks, Hermannsburg (Kempe),
by the Finke near Mount Sonder and by the Hugh at Alice Well!; also Crown
Point and Stevenson River !.

Newcastiia spopiorricua, & v. JZ. McDonnell Range (E. Giles); sandhills,

Hermannsburg (Kempe).

Newcastiia BRActeosa, /. v. AZ. Gill and McDonnell Ranges, also between
Mount Olga and Warburton Range (E. Giles).

DicrastyLis Doran, / v. M. Hermannsburg (Kempe). Sandhills and
plains; Eagle Plain by Palmer River, Reedy Creek, between Glen Edith and
Carmichael Creek, Ooraminna Pass, Deep Well, and thence south to between
Boggy Flat and Charlotte Waters!, Stony ground, slopes of Mounts Tate and
Sonder, Stuart’s Pass!. Flowers blue.

DicRASTYLIS ocHROTRICHA, &. v. AZ. Laura Vale (Tietkens), Ilpilla Gorge,
Bagot’s Creek and Mount Sonder!. Extends to Barrow Range (E. Giles), and
Victoria Desert (Elder Exped.).

DiorastyLis GILEsil, / v. AZ. Glen of Palms (E. Giles); also Mounts Olga
(E. Giles) and Conner (Tietkens).
DicrastyLis BeveripeGet, & v. 47. Between Mount Udor and George Gill

Range ; also Mount Olga (E. Giles).

DicrastyLes Lewewiint, 7: v. JZ. McDonnell Range (E. Giles). Sandhills
(Kempe), Missionary Plain !.

HORN EXPEDITION— BOTANY. 17

wt

CLERODENDRON FLORIBUNDUM, &. Brown. Hermannsburg (Kempe); Laura
Vale and Watson Hills (Tietkens). Sandhills between Laurie’s Creek and Glen

Edith. Source of Darwent River, Mount Francis, Mount Sonder, Horn Valley !.

MYOPORINA.
* EREMOPHILA STRONGYLOPHYLLA, /. v. AZ. Throughout George Gill Range !.

Eremopnita Mircnerni, Lertham. Hermannsburg (Kempe). Sandhills and
plains ; Bagot’s Creek, Hope Valley, Glen Edith to Carmichael Creek, Ooraminna

Pass and thence to Charlotte Waters !.

Eremopuita Paistryi, % v. JZ. Sandhills at Idracowra and between James
Range and Alice Creek !; also west end of Lake Amadeus and south-west of
Erldunda (Tietkens).

Eremopuita Strurti, A. Lrowr. McDonnell Range (E. Giles) ; Hermanns-

burg (Kempe) ; Idracowra!.

Eremopnina Crarker, 2 v. JZ. Warman Rocks (Tietkens), [pilla, Reedy

Creck, Mereenie Bluff and scrub south-west of, Glen Helen, Ooraminna Pass !.

Eremopmina Ginesi, /. v. JZ. MeDonnell Range (BE. Giles); Warman
Rocks (Tietkens). _[lamurta !.

Eremopuita Larrosnr, & v. AZ. McDonnell Range (E. Giles); Hermanns-
burg (Kempe), Laura Vale and Warman Rocks (Tietkens). Hamurta and south
side of George Gill Range !.

Var. (= Tiethenst, Fv. M. and Tate). Mount Sonder and Laura Vale

|
(Tietkens), Ipilla Gorge and south side of George Gill Range !.

Eremopnina Lonarroura, 72 v. AZ. McDonnell and Gosse Ranges (EK. Giles).
Sand plain off George Gill Range, valley of Carmichael Creek, foot slopes of
Mount Sonder and elsewhere !.

TREMOPHILA FRreevinci, 7/2 v. AZ Hermannsburg (Kempe). Common on

stony ground from the southward to Chandler Range ; frequent on the tablelands

as at Hlamurta, Tempe Downs, George Gill Range, ete. !.

Eremopuita Macponnewul, “v7. JZ Hermannsburg! (Kempe). Common,
on sandy ground from the southward to the junction of the Finke and Palmer

tivers ; valley of Alice Creek !.

176 HORN EXPEDITION—BOTANY.

*Eremopuita Goopwinu, / v. JZ. Glen of Palms and McDonnell Range
(E. Giles). Rocks and rocky ground, Parke’s Gap, Ipilla, slopes of Mount Tate,
Horn Valley, Finke Gorge, Stuart’s Pass !.

Eremopnina Winisu, / v. AZ. Finke River (Stuart), Hermannsburg
(Kempe), Chambers Pillar !, ete.

EREMOPHILA PLATYCALYX, / v. JZ. North-west interior of South Australia
(Stuart).

Eremopnita Brown, / v. A. McDonnell Range (Stuart), Missionary

Plain !, near Hermannsburg (Kempe), Alice Creek !.

Eremopuita Durroni, “/ v. AZ. From Sullivan’s Creek to Idracowra ;
Tlpilla, Tempe Downs, Heavitree Gap (with yellow flowers), Ooramitina and south
to Alice Creek !.

EremopuHiLa MAcuLATA, 2. v. A/. North of Mount Harris (Tietkens), Eagle
Plain by Palmer River !.

ErREMopPHILA CuristopHort, / v. AZ River Hugh (C. Giles); foothills of

Mount Sonder !.

Myoporum Dampirrt, Cunn. Glens of Palms (KE. Giles), Hermannsburg
(Kempe). River Finke at Running Water; Tempe Downs; Goyder Pass, Finke

Gorge !. Drupes red.

ASPERIFOLIA.

*CynoaLtossuM DrumMonpil, Bentham. Hermannsburg (Kempe). Rock-

slopes, Ilamurta, Stokes Pass, Horn Valley and Finke Gorge !.

|| PotnicniA ZeyLanica, /. v AZ. Mostly on stony ground, and ascending to
high elevations on the tablelands and other eminences throughout the Larapintine
area! (recorded by E. Giles, Kempe and Tietkens). In the region to the south it

occurs more frequently on the sandhills !.

Hanaania cyaneA, Lindley. Brinkley Bluff (Stuart), McDonnell Range
(E Giles). Ranges and sandhills by Hermannsburg (Kempe). Slopes of Mounts
Tate, Sonder and Gillen, Stnart’s Pass, Alice Springs. Sandhills, valley of the

Lower Hugh River and thence to Charlotte Waters !.

HALGANIA INTEGERRIMA, Zvd/. Mount Harris (Tietkens).

~I
com j

HORN EXPEDITION—BOTANY. i

Herriorropium pLeropreruM, 727. JZ Sandhills by Hermannsburg (Kempe),
Tdracowra and Chambers Pillar; junction of Palmer and Finke Rivers; Alice
Creek, the Lower Hugh River and thence to Engoordina !.

| Heriorroprum Curassavicum, Zzzné. Margin of the Finke River in the

Finke Gorge !, at Hermannsburg (Kempe), and also at Crown Point !.

| Heriorropium unpuLatruM, Vaf?. Hermannsburg (Kempe). Between

Henbury and Parke’s Gap, Redbank Gorge, Mount Francis !.

Heiorropium AsperrimuM, &. Lrowz. McDonnell Range (KE. Giles),
Ifermannsburg (Kempe), Laura Vale (Tietkens); also Crown Point and at
the Goyder River}.

/Hrniorropium ovaLirotium, /orske/. Slopes of Mereenie Bluff!; also at
Lake Macdonald (Tietkens).

HELIOTROPIUM FILAGINOIDES, Bentham. Lake Macdonald (Tietkens). Near
Charlotte Waters (E. Giles).

HeLiorrorium PANICULATUM, 2. Brown. Mount Sonder! and Painta Spring
? ?
(Tietkens). Mount Francis and Stuart’s Pass !. Common on sandy alluvium from

the Goyder River to Macumba.

EPACRIDEA.

*SrypHeLiA Miroenevui, /. v. 4 At high elevations on Mount Sonder !.

PEDALINEA.

JosmPpHiIna Eucentm, “ v. JZ = Watson Hills (Tietkens). Also sandhills

by the River Stevenson near Macumba!.

CONIFERA.

*CaLLitRIs verrucosa, 2. Lrown. Strictly saxatile in habitat, and always
of the smooth-coned variety. Chandler's Range (the most southern station
observed), thence widely spread to the western and northern confines of the

Larapintine region !. Recorded by E. Giles and Kempe.

CYCADEA.

* ENCEPHALARTOS MacponneLu, / v. JZ. Brinkley Bluff (Stuart), Stuart’s

iT

Pass, and in the bed of the Hugh north of Paisley Bluff! Penny Springs !

99
20

in

178 HORN EXPEDITION—BOTANY.

George Gill Range (E. Giles). Krichauff Range (Kempe) and Palm Creek off
Glen of Palms!. Mount Sonder and Heavitree Gap!. Always gregarious and

saxatile.

Macrozamia Macdonnelli was the name given to a cycad, collected by Stuart
in Central Australia, by F. v. M. in Frag. Phyt. Aust., vol. ii, p. 179, and
attributed to the locality, River Neale. Stuart in his “ Journals of Explorations ”
makes no reference to the plant as from there, but at p. 157 (2nd edit.), he
describes a cycad calling it a palm tree, which leaves no doubt that the original
specimens came from Brinkley Bluff, where I have actual knowledge of its
occurrence. Moreover, F. v. M. in the “ Enumeration of the Plants,” p. 505, of.
cit., states that “a cycadeous plant occurs on McDonnell Range,” and makes no
allusion to the River Neale, which is several hundreds of miles south of the most
southerly station actually known. By this correction the species is restricted to
the George Gill, Krichauff and McDonnell Ranges.

Stems attain to four feet high with a diameter of eighteen inches, the longer

gonal and concave above, and

<

leaves measure ten feet in length, the petioles tri
bear from ninety to one hundred pairs of leaflets. The leaflets are flat, margin
entire, the larger ones about one foot long and one-quarter inch wide, the lower
leaflets gradually shortened, but none reduced to spines, the basal eighteen
inches of the petiole without leaflets, attenuated to a slight pungent point, the
upper surface obscurely seven- to nine-veined, and the interstitial spaces with
distant granulose streaks ; the base of the leaflet with a relatively large articular

callosity, suddenly contracted above, the insertion marginal and axial.

Male cones ellipsoid-cylindrical, twelve inches long by three and a quarter
inches wide ; antheriferous scales very numerous and thick, the lower ones blunt
and abbreviated, those towards the middle short-pointed, those towards the summit
with vertically ascendent apices, the longest of which is three-quarters of an inch
and the attenuated point is somewhat pungent. This species was associated by
Mr.- Bentham, Fl. Austral., vol. vi. p. 253, with Z. #raser?, but it differs from it
and therefore from £. spiralis by the rachis not being raised between the pinne.
The male cones of £. Macdonnelii, hitherto undescribed, are equally large as those
of £. Fraseri; but its upper scales have not the long subulose tips of that species.

HYDROCHARIDEA.

OrreLiA ovaLirouia, LZ. C. Richard. Rock pool in Reedy Creek Gorge,

George Gill Range!. All the plants exhibit an extreme of dimorphism, which

HORN EXPEDITION—BOTANY. 179

was pointed out as pertaining to this species by F, v. M. in “ Key to the Victorian
Plants,” i, p. 422, and more fully dealt with in the “‘Gardener’s Chronicle.” In
the Reedy Creek plants, the perianth is almost obliterated and uncoloured, and

the spathe always remain perfectly closed.

AMARYLLIDEA.

CrinuM FLAccIDUM, /fervert. Latitude 52° to 22° (Stuart). Near McDonnell
Range as C. angustifolium (teste F. v. M.). Common in the valley of the

Stevenson River !.
LILIACEA.
WurmbsEA pbioica, / v. AZ. Glen Edith, etc. (Tietkens).
THYSANOTUS EXILIFLORUS, 7) v. JZ. McDonnell Range (E. Giles); sandhills,
Hermannsburg (Kempe).
CorYNOTHECA LATERIELORA, /. v. JZ, Sandhills, Hermannsburg (Kempe).
* XeRores DuRA, Z. v. AZ. In rocky clefts, Ilpilla Gorge and Palm Creek |.

XEROTES LEUCOCEPHALA, 2. Lrown. Sand plain by the Finke, Hermanns-
burg! (IXempe), Gill’s Creek and Laura Vale (Tietkens), Walker River valley near

Palner Junction !.

XANTHORRHGA THorntToNI, Za/e, n. sp. Sandhills, Eagle Plain; between
Laurie’s Creek and Glen Kdith!, as observed by Gosse ; Rudall’s Creek (1. Giles).
Missionary Plain one mile north of Pine Point, and south side of valley of

Carmichael Creek !.
PALMA.

* LivisronaA Marin, & v. AZ, Glen of Palms (E. Giles), along the Finke
fiver and some of its tributaries in Krichauff Range (Kempe). The principal
colony of this stately palm, which attains to a height of ninety feet, is in Palm
Creek, which joins the Finke at about nine miles south from Hermannsburg ; the
trees, rooting in the joints of the bare sandstone floor of the creek-bed, extend
for a length of about two miles, commencing at about three miles from its junction
with Glen of Palins, altogether there cannot be more than about a hundred full-
grown individuals ; the tributary-branches of Palm Creek have a few individual
trees but not extending beyond one-fourth mile from the main creek. rom
Palm Creek a few individuals occur along the Finke Channel as far as Boggy
Water in the Glen of Palms. 234

180 HORN EXPEDITION—BOTANY.

This species has been recorded as inhabiting a very circumscribed area in the
valley of the Fortescue River (F. v. M., in ‘“‘ Plants of N.W. Australia,” Perth,
1881, p. 12), but further material has proved that the fan-palm of West Australia
is distinct and it has been named Z. A/fredi (F. v. M. in Victorian Naturalist,
December, 1892).

TYPHACEE.

| TypHA ANGUSTIFOLIA, Zizné. Hermannsburg (Kempe); Illara Water, Tempe
Downs, Bagot’s and Reedy Creeks, Palm Creek !.

FLUVIALES.

| Natas mAgor, Addioni. River Finke at Running Water, Palm Creek ! near
Hermannsburg (Kempe); Illara Water, Bagot’s Creek !.

PoramoceTon TrEppert, A. Bennett. Finke River at Henbury and Running
Water; Reedy Creek ; Palm Creek off Glen of Palms !.

TRIGLOCHIN CALCITRAPA, /Zooker. Palm Creek, Carmichael Creek !; also by

the Stevenson River !.

TRIGLOCHIN MuUCRONATA, &. Grown. Clay-banks of Finke River at Henbury!.

COMMELINEA.

* CoMMELINA ENSIFOLIA, &. Lrown. McDonnell Range (Stuart); Glen Helen
(Tietkens). Shady places, Hermannsburg (Kempe). Alice Springs (F. J. Gillen!).

JUNCACEA.

Juncus pALLipus, &. Brown. lllara Water; Bagot’s, Reedy. and Penny
Creeks in George Gill Range ; River Finke by Mount Sonder'!.

ERIOCAULEA.

ERIOCAULON GRAPHITINUM, /. v. JZ. and TZate. West end of McDonnell
Range (Tietkens).

RESTIACEA.

CENTROLEPIS POLYGYNA, //zer. Palm Creek and Conlin’s Lagoon}.

HORN EXPEDITION—BOTANY. 181

CYPERACEA.
Cyperus squarrosus, Zinné. Henbury, Bagot’s Creek, Carmichael Creck,
Upper Finke by Mount Sonder and Palm Creek !.

| Cyperus pirForMis, Zizzé. Glen Helen! (Tietkens), Henbury and Car-
michael Creek !.

Cyperus vaacinatus, 2. Brown. McDonnell Range as C. fextilis (KE. Giles),
Hermannsburg (Kempe), Alice Springs (C. Giles).

Cyperus FuLvus, A. Lrown. Glen Helen (Tietkens), Reedy Creek,
Engoordina !.

|| Cyperus rotunbus, Zinné. Charlotte Waters and Alice Springs ! (C. Giles).
Loam-flats of the River Finke at Crown Point, Henbury, ete !.

Cyererus susuLatus, 2. Brown. Alice Springs (C. Giles).

*| CypERUS UMBELLATUS, Bentham, f., Hongk., 386, on rocky slopes of Mount
Tate and in Stuart’s Pass !.

[The Central Australian plant can be distinguished from the typic form as
var. fasctcudigerus, inasmuch as the spikes are shortened almost all to fascicles
with a tendency to ramification. But similar variations nay be observed in some
other species of Cyperus, for instance our C. Zucidus. The plant before us has the
radical and floral leaves also narrower than usual, which is doubtless from the
effect of desert clime. F.v. M |] The whole plant is very viscid.
| Heteocuaris acuta, A. Brown. Carmichael Creek!; also at Opossum
Waterhole, River Stevenson !.

|| Heteocuaris capirata, 2. Brown. Palm Creek !.

| FimpristyLis AcuMINATA, Vaid. West end of McDonnell Range (Tietkens),

| FimBristyLis CoMMUNIS, Auth. Gill's Creek (Tietkens). Sandy loam flats,
widely spread |.
| FIMBRISTYLIS FERRUGINEA, Vah/. Finke Gorge (with minutely hoary
pubescent glumes) !.
|| FIMBRISTYLIS BARBATA, Letham. Between Alice Springs and Charlotte
Taters (C. Giles).
Wat C. Gil

!

|Scirpus riparius, Sprengel. Conlin’s Lagoon and Goyder Pass !.

182 HORN EXPEDITION—BOTANY.

|| Scrrpus supinus, Zizzé. Reedy and Carmichael Creeks !.

Scirpus puNGENS, Vad. Illara Water and Palm Creek !.

| Scirpus LiToRALIs, Schrader. Palm Creek !, Hermannsburg (Kempe),
lara Water !.

|| LipocARPHA MICROCEPHALA, 2. Lrown. Carmichael Creek and Stuart’s

FUIRENA GLOMERATA, Lamarck. West end of McDonnell Range (Tietkens).

GRAMINEZA.

|| Er1ocHLoa potystacuya, /Z. and A. Hermannsburg (Kempe). Engoor-

dina and southward to the Macumba !.

Panicum bivAricatissimuM, 2. Brown. Hermannsburg (Kempe) ; Running
Water !.

|| PANIcuM LeucopHa@uM, AZ. and A. Hermannsburg (Kempe). Running
Water and common throughout the region !.

PANICUM ARGENTEUM, 2. Grown. Near Hermannsburg (fide F. v. M.).
Panicum GRACILE, 2. Grown. East end of George Gill Range !.
Panicum HELOPUS, Zyiz. Henbury, also Crown Point !.

Panicum Giuesil, Aextham. UWermannsburg (Kempe); also Charlotte
Waters (C. Giles).

| Panicum pistacuyon, Zinxzé. Hermannsburg (Kempe).

Panicum PAUCIFLORUM, &. Brown. In the interior (Stuart), near Alice
Springs (C, Giles).

| Panicum DEcompPosituM, &. Lrown. Hermannsburg (Kempe), Glen Helen
(Tietkens), Bagot’s Creek !.

| SerariA MAcRosTAcHyA, /7, and A. Hermannsburg (Kempe).

| Serarra viripis, Padisot. McDonnell Range (Giles). By nearly all river
banks in the region !.
PENNISETUM REFRACTUM, / v. JAZ. Alice Springs (Giles). Banks of the

Finke at Idracowra and Crown Point !.

HORN HEXPEDITION—BOTANY., 183

SPINIFEX PARADOXUS, Ftentham. Alice Springs (Giles), Hermannsburg
(Kempe) ; plain off George Gill Range, ete. !.

| Prrotis rARA, XR. Brown. Hermannsburg (Kempe); Ipilla Creek and at
Alice Springs !.

| Tracus racemosus, /aller. McDonnell Range (E. Giles), Hermannsburg
(Kempe). Hpilla and throughout the region !.

* NEURACHNE ALOPECUROIDES, &. Lrown. Stony slopes in the Ipilla Gorge !.

| IMpPERATA ARUNDINACEA, Cy77//o. Hermannsburg (Kempe). Tlamurta

Soakage and Tempe Downs !.

ErIANtTHUS FULVUS, Avvth. Bagot’s Creek, and in ravine on south side of
Mount Tate |.

| ANDROPOGON ANNULATUS, Zvrsk. Reedy Creek in George Gill Range !.
| ANDROPOGON sERICEUS, A. /rown. Hermannsburg (Kempe).

| ANDROPOGON PERTUSUS, IT7//d. South side of George Gill Range, also at
Crown Point !. Extends to Mount Olga (E. Giles).

ANDROPOGON EXALTATUS, RK. Brown. Hermannsburg (Kempe) ; Ipilla Gorge
and Tempe Downs}.

* ANDROPOGON BomMBycINUS, 2. Brown. McDonnell Range (Stuart); Mount
Zeil (Tietkens). Tpilla Gorge, Tempe Downs, Mount Tate and Mount Francis !.

| ANDROPOGON GryLLus, Zizé. Alice Springs (C. Giles). Alluvial flats and
river margins, Running Water, Ipilla, [lara Water, Tempe Downs, Carmichael

Creek, Upper Finke by Mount Sonder, Horn Valley, Alice Creek !.

| ANTHISTIRIA CILIATA, Livné. Hermannsburg (Kempe). Running Water,

Tempe Downs, Mount Francis, ete., chiefly on rocky slopes !.

ANTHISTIRIA AVENACEA, 7. 7. AZ. Root-stock densely silky-hairy. Loamy
plains and flats, south side of George Gill Range, Hope Valley, Glen Edith and
Horn Valley!.

AriIstipA stipoipres, 7. row. Hermannsbure (Kempe), between Alice

) 5 ] ’
Springs and Charlotte Waters (C. Giles). Mulea serub near source of Carmichael
pring g
Creek !.

ARISTIDA ARENARIA, Gauvd. Between Alice Springs and Charlotte Waters

(C. Giles). Common throughout the region !,

184 HORN EXPEDITION—BOTANY.

AnrisTIpA RAMosA, 2. Brown. Hermannsburg (Kempe).

ARISTIDA CALYCINA, 2. Brown. Hermannsburg (Kempe); near Alice Springs
(C. Giles), Glen Helen and Tempe Downs !.

Stipa scapra, Livd/ey. HKdgar Spring, a tributary source of Harris Creek !.

PAppopHoRUM comMUNE, / v. JZ. McDonnell Range (E. Giles); Ranges,

Hermannsburg (Kempe). Not infrequent throughout the region !.
| Sporopoius InNpicus, R. Brown. Alice Springs (C. Giles).

Sporonpotus Linpieyi, Lentham. Hermannsburg (Kempe); Glen Helen
(Tietkens), Idracowra |}.

SPOROBOLUS ACTINOCLADUS, /. v. AZ. Idracowra!.

EriacuHneE Aristipgea, / v. 47. Common on the Triodia sandhills and plains
north and west of Engoordina, to the south side of George Gill Range and

Ooraminna Pass, also south as far as Crown Point! and Charlotte Waters

(C. Giles).

* ERIACHNE SCLERANTHOIDES, /. v. AZ. McDonnell Range (E. Giles). Ipilla
Gorge, Tempe Downs, Mount Tate, Mount Gillen !.

DANTHONIA BIPARTITA, /. v. 14, Between Ooraminna and James Ranges !.

ASTREBLA PECTINATA, /. v, MZ, Deep Well in James Range to Alice Creek.
Also stony tablelands south from Charlotte Waters !.

CuLoris AcicuLaAris, Lindley. Alice Springs (C. Giles), Hermannsburg

(Kempe). Also Crown Point, Charlotte Waters, and creek margins southward !
Cuioris truncata, A. Brown. Hermannsburg (Kempe).
|| CHLorIs BARBATA, Szvarts. Carmichael Creek and Alice Springs!; also
River Stevenson (Stuart).
Cuioris scartosa, / v. 47. Glen Helen |}.

| ELeustnk cructata, Lamarck. Hermannsburg (Kempe), and common

throughout the region !.

ELEUSINE Dicirata, Sprengel. McDonnell Range (E. Giles). Banks of the
tiver Finke at Engoordina, and by Mount Musgrave in the Finke Gorge ; also

Adminga Creek !.

HORN EXPEDITION—BOTANY. 185

|| DIpLACHNE LoLitForMis, 2 v. AZ, Between Alice Springs and Charlotte
Waters (C. Giles), as at Mount Squire near Engoordina !.

| Diptacnnr rusca, Pa/iso¢t. River Finke at Finke Gorge and Henbury |,

also River Stevenson !.

Triopia PUNGENS, 2. Lrown. The chief vegetation of the rocky tablelands

and hill slopes.

Triopia IRRITANS, #. Frown. Ubiquitous (Kempe). Also sandhills as far

north as Macumba!.

The porcupine grass was seen rarely in flower, and then always with the floral
characters and viscid leaf-sheaths of 7: pungens ; if one may judge of the species by
the presence or absence of a viscid exudation, then the ubiquitous species is
T. pungens and not ZT. irritans; indeed I have not observed 7. 7rritans as a
saxatile species, if at all, even in the Larapintine region. Bentham in FI. Aust.,
vol. vii., pp. 606 and 607, indicates Z. pungens as a more northern species
than 7. zrritans, whilst the latter is “probably the ‘porcupine grasses’ of the
southern interior deserts of Australia ;’ my observations are in accord therewith,
and T am afraid that Mr. Kempe’s determination is in the main, at least, incorrect.
The young leaves in life are flat and copiously covered with a varnish, which for
its tenacious adhesiveness may be compared to copal varnish ; on drying the leaves
roll up into a cylinder, and with age the same thing happens concurrently with the
disappearance of the viscid exudation from the surface of the leaves, though some

may be retained on the less exposed leaf-sheaths.

Triopia sp. (? Z. Mitchel, Bentham). ‘“ Old-man porcupine.” — Forming
exceedingly large tussocks, up to eight feet high and twelve feet diameter, foliage
of a dull ashen grey ; flowers not seen. Tempe Downs, Rudall Creek by Mereenie

Bluff, under Mount Sonder !, Palmer River (Spencer).

| ERAGROSTIS TENELLA, Padisot. McDonnell Range and Charlotte Waters
(C. Giles). Henbury, Running Water and Reedy Creek !; also Stevenson River !

(Stuart) and Giddea Creek near Oodnadatta !.
ERAGROSTIS TRICHOPHYLLA, Bentham. No locality (Tietkens).
ERAGROSTIS DIANDRA, Sfevde/. Glen Helen (Tietkens); Carmichael Creek !.
| Eracrostis Brownu, ees. Hermannsburg (Kempe).
Eracrostis speciosa, Stevde/. Running Water by banks of Finke River !;

also at the Goyder River! and Hamilton River (Stuart).

186 HORN EXPEDITION—BOTANY.

ERAGROSTIS LANIFLORA, Lentham. Common on sandy ground among 7Zyiodia,
Idracowra and northward, plain off George Gill Range !.

ERAGROSTIS ERIOPODA, Bentham. Bagot’s Creek !.

ErRAGROSTIS FALCATA, Gaud. Alice Springs and Charlotte Waters (C. Giles) ;
also at the Goyder and Stevenson Rivers !.

TRIRAPHIS MOLLIS, 2. Brown. Alice Springs and McDonnell Range (Giles).
Widely dispersed throughout the district, also at Crown Point !.

TRIRAPHIS PUNGENS, 2. Brown. Bagot’s Creek Gorge!; has the habit of
Triodia pungens, the leaf-sheaths are slightly woolly.

|| ARuNno Puracmites, Zizné. Hermannsburg (Kempe). Henbury; Bagot’s,

Reedy and Palm Creeks !.

RHIZOSPERMEA.

|| MARSILEA QUADRIFOLIA, Zinné. Clayey banks of creeks and loamy flats

subject to inundation, widely diffused !.

LYCOPODINA.

*|| PsILorUM TRIQUETRUM, Szartz. Rocky clefts over-hanging rock-pool at
Reedy Creek !.

FIILICES:

*|| LyGoDIUM RETICULATUM, Schkuhr. McDonnell Range (fide F. v. M.).

*

| ADIANTUM HISPIDULUM, Szvartz. Rocks by waterhole at Reedy Creek !.

*

|| CHEILANTHES VELLEA, / v. JZ. McDonnell Range (KE. Giles), Krichauff
Range (Kempe), Mount Sonder (Tietkens), Mount Tate !.

*

| CHEILANTHES TENUIFOLIA, Swartz. A common rock-fern throughout the
region !. Recorded by Kempe and Tietkens.

|| ASpiprum unriruM, Swartz. Marsh by waterhole Reedy Creek, and by
Penny Springs in Penny Creek |.

*Grammitis ReyNnoupsu, / v. MZ. Shaded rocks in Stuart’s Pass !.

*||GRAMMITIS RUTHFOLIA, 2. Brown. Finke Gorge}.

HORN EXPEDITION—BOTANY. 187

6. DIAGNOSIS OF NEW GENUS AND SPECIES.
Acacia CowLEaANna, Tate.

Slender, erect, about six to eight feet high ; the foliage and young branchlets,
ashy or hoary with very minute appressed hairs. Branchlets stout, acutely
trigonous. Phyllodia lanceolar-falcate, narrowed at both ends, mostly five to
seven inches long and three-fourths wide at the middle, coriaceous, with three
prominent parallel veins, the interspaces with eight to ten secondary veins which
frequently anastomose. Stipules minute lanceolate. Spikes shortly pedunculate,
one or two together, up to two inches long. Flowers distant or distinct,
pentamerous. Calyx very much shorter than the corolla, minutely pubescent,
with five short blunt denticulations,

Corolla deeply five-cleft, smooth; each segment narrow, oblong, with an
apiculate tip; yellow, brown at the base.

Ovary pubescent. Pod (not seen ripe) exceedingly flat, long and narrow,

four to five inches long, and one-seventh wide, not twisted, glabrous or nearly so.

Seeds longitudinal ; funicle very long and slender, loosely double-folded at
about the middle, beneath the seed.

The species name is in compliment to Trooper Cowle, who conducted a section
of our party to Mount Olga, and in various other ways promoted the scientific
objects of the Expedition.

Among members of the series Juliflorz, this new species finds a place in the
section Faleate near to A. glaucescens and A. Cunninghamii ; from the second it
differs by its straight pod and thus resembles the former; from A. g/aucescens ib
differs by its very long smooth pod, oblong-apiculate petals and by coarser

anastomosing secondary venation.

ACACIA FRUMENTACEA, Tate.

A small tree attaining ten or fifteen feet high, glabrous and mealy glaucous ;
branchlets somewhat angular. Phy/odia narrowly oblong, apex obtuse, with a
minute tip recurved over a subterminal gland, narrowed at the base, two to three
inches long, coriaceous, with a prominent mid-rib and distinct reticulate veins,
pale green. Peduncles slender in axillary racemes, shorter than the phyllodia ;
heads globular of about forty flowers, mostly tctramerous. Sepals very narrow

linear, slightly spathulate at the end, smooth, free. eéa/s distinct or almost so,

244A

188 HORN EXPEDITION—BOTANY.

smooth, lanceolate-oval to oval-oblong, about twice as long as sepals. Pod oblong,
flat, obtuse, one and half inches long by one-quarter or three-eights wide ; valves
membranous. Seeds about six, transverse, thick, depressedly orbicular to oval-
oblong, impressed above and below; estrophiolate ; funicle short, once or twice

folded under the seed.

This species in its foliage, flowers and fruit approaches A. /eAfofetala, but
seems to differ by more distinct neuration of the phyllodia, by its tetramerous
flowers and flattened seeds. It has some affinity with A. senfis, but the seeds are
not globose, and stipules are absent.

Dipiscus GiLLEN#, Tate.

Herbaceous, apparently annual, acaulescent with radical erect leaves and
decumbent simple peduncles, spreading to one or two feet; when dwarf the peduncle
is erect. Leaves on long petioles, deeply five-lobed with cuneate three- or five-lobed

divisions, sparsely covered with long soft hairs.

Peduncles two or three times exceeding the leaves, simple; umbel of numerous
flowers on relatively long pedicles. Involucral bracts herbaceous, linear-lanceolate
with setiferous tips and margins, as long as the flowers and distinctly united at

the base.

Flower-head 10 to 20 mm. diameter; flowers very numerous on slender
pedicles of 5 or more mm. long, calyx tube red; petals whitish above and pink

beneath ; anthers red.

Fruiting pedicels exceeding the involucral bracts; carpels slightly laterally
compressed, densely covered with simple bristly pinkish-red hairs having a
thickened base; one carpel usually larger than the other, oval, about 2 mm.

high and less in width ; seed slightly compressed.

In its bristly carpels this new species resembles D. cyanopeta/a from which it
differs in denser umbels, well-developed pedicels, longer leaf-stalks, colour of flowers

and carpels.
The dedication is a slight mark of tribute to Mrs. F. J. Gillen’s hospitality,

which was enjoyed by the author and other members of the Expedition.

WEDELIA STIRLINGI, Tate.

Erect, rigid, often two feet high. Leaves linear-lanceolate, acuminate, toothed.

Peduncles rigid, up to six inches long, solitary. Involucres hemispherical, about

HORN EXPEDITION—BOTANY. 189

quarter-inch diameter, the bracts oblong acute. Ray-florets quarter-inch long.
Scales of the receptacle acute. Achenes winged and tuberculate. Pappus not

cupped, reduced to a bristle or two at the end of the wings.

This new species belongs to that group in which the outer involucral bracts
are similar to the inner ones, and of these to those in which the pappus is reduced
to one or two bristles. It, however, resembles most IV. spilanthoides in its long
rigid solitary peduncles. From IV. d¢fora and IV. asferrima, it is separable among

other characters by the winged and tuberculated achenes,

GoopDENIA Horniana, Tate.

Stem erect, woody, usually branched, not exceeding one foot. Leaves softly

but minutely glandular-pubescent or tomentose, rhombic-oval, coarsely serrate

5 ? ) ’

half to three-quarter inch diameter, on petioles about as long as the blade.
) I 8

Peduncles axillary, slightly shorter than the leaf-stalks, one-flowered, with a slender
? 5 ? ) 5)

linear bracteole below the middle. | Calyx-lobes linear-lanceolate, glandular-pubes-

cent. Corolla large, about one inch long, bluish-white streaked with purple, silky

pubescent outside, hirsute inside, but the auricles smooth inside and outside; the

two upper lobes more deeply separated, all the lobes broadly membranously winged,

the adnate part of the tube with a slight baccate protuberance. Style almost as

long as the corolla, silky-hairy throughout its length; stigmatic cover purple,

smooth or with a few hairs at the base, fringed with short erect white hairs at the

orifice. Capsule about half-inch long ; dissepiment reaching about two-thirds the

length of the capsule; seeds several in two rows, small, orbicular, flat, shining

fo) p d d ’ 2 oD

brown, minutely granular, with a narrow smooth thickened margin.

This species comes near G. grandiflora and G. Chambersit, from which it con-
spicuously differs by the violet (not yellow) colour of its flowers and by the presence

of distinct bracteoles.

GoopENIA Lanrapintra, Tate.

An erect, unbranched, viscid-villous herb, about one foot in height. Leaves
oval-lanceolate, distinctly serrate, sessile. Peduncles one-fowered, axillary, longer
than the subtending leaves. Bracteoles none or filiform and minute. Calyx-lobes
linear-lanceolate. Corolla about half-inch long, the three lower lobes broadly
winged ; the two upper ones separated much lower down than the others, shorter,
narrower, less broadly winged, but with an auricle on the outer margin below the
smooth ; the stigma cover smooth, except

middle. Style under quarter-inch long,

190 HORN EXPEDITION—BOTANY.

a few scattered white long hairs and the terminal fringe of dense short ones.
Capsule cylindrical, oval-oblong, half-inch by quarter-inch ; dissepiment fully half
as long; seeds small, several lenticular, dark brown, minutely granulated, with a
narrow thick whitish margin.

This species has the habit and the floral characters of G. heterochi/a, but its
viscid foliage approximates it to G. sefalosa, though it has not the leafy calyx-lobes
of that species. It differs from both by its cylindrical capsule, relatively long
dissepiment, lenticular (not flat) seeds and corolla-lobes not so much dissimilar.

Elacholoma. F. v. M. and Tate.

Calyx campanulate-ovate, its five lobes much shorter than the tube. Corolla
filiform-tubular, very much narrower than the calyx, widened only at the
summit; lobes minute, almost inperceptible. Stamens two, short-exserted; anthers
almost reniform, ex-appendiculate, dorsi-fixed, bursting anteriorly, their two cells
confluent. Style fully as long as the corolla, very thinly filiform. Stigmas two,
conspicuous, divergent, capillulary. Ovulary two-celled, without any parietal
intrusion beyond the dissepiment. Placentaries axillary, somewhat projecting.
Capsule turgidulous-oval, loculicidal-dehiscent. | Seeds numerous, very minute ;

hilum basal ; albument conspicuous ; embryo straight.

A minute annual herb, whitish-grey from tomentellous vestiture; leaves
linear, scattered or the lower opposite; flowers sessile, axillary, solitary but
somewhat crowded at the summit of the stems.

Exacnotoma Horn, F. v. M. and Tate.

An erect or diffuse herb, four inches or less high. Root rather copiously
fibrous. Leaves extremely narrow, hardly acute, slightly kelled, concave above,
flaccid, from one-third to two-thirds of an inch long. Calyces measuring about
one quarter of an inch in length, longitudinally five-streaked ; their lobes deltoid
semi-lanceolar, finally converging. Corolla glabrous, seemingly dark-coloured ; its
upper portion emerged. Stamens, ovulary and style glabrous. Stigmas subtle-
papillular. Capsule about one-sixth of an inch long; the pericarp of almost
membranous texture, its dehiscence nearly bivalvular. Seeds brown, truncate,
ovate, almost smooth. Embryo nearly ellipsoid.

This Scrophularinous genus recedes from all others of that order in the extra-
ordinary thinness and almost lobelessness of the corolla within an inflated calyx,
and differs more particularly still in its comparatively long and quite capillulary

stigma divisions, by which some approach of this genus to the Sesameve is indicated.

HORN EXPEDITION—BOTANY. 191

XANTHORRH@A THorntont, Tate.

Caudex attaining to a height of six feet and a circumference of three.
Leaves slender but rigid, four feet long, strictly quadrangular, about two milli-
metres in diameter, interstriated (about nine strize on each face); margins acute,
minute crenate-serrate. Scape seven feet long, inclusive of the spike which is five
and a half feet. Inner bracts crustaceous, oblong, obtuse, undulate on the margins,
smooth and shining, without veins, about half the length of the capsule. Outer
bracts linear with spathulate tips, without veins ; the outermost ones with broadly
decurrent bases. Flowers not seen. Capsule one inch or more in length; the
valves broadly lanceolate, abruptly narrowed into a long somewhat pungent-pointed
tip ; the upper-half of the outer face finely longitudinally furrowed. Seeds oblong-
elliptic in longitudinai outline, acutely triangular in transverse section, black,
minutely granulated ; outer face convex, longitudinally ridged ; the inner narrow

faces separated by an acute medial ridge.

The species name is in compliment to Mr. Thornton, late of Tempe Downs,
who at considerable trouble was the first to bring this grass-tree to my notice, and

in other directions greatly forwarded the objects of the Expedition.

This species by its foliage resembles the southern X. guadrangulata, from
which it conspicuously differs by its seape, very much shorter than the spike ; also
by its longer and narrower capsule, and relatively shorter subtending bracts.
X. Preissit, to which it is geographically nearest, is somewhat intermediate
between X. Zhorntont and X. guadrangulata as regards the proportionate length
of the flower-bearing portion of the scape ; but the foliage among other characters

is different.

Cuaprer I]1.—The Central Eremian Flora.

l. PHystocrapinic aND BoTanic CHARACTERISTICS OF THE REGION.

That portion of the central EKremian region travelled over by the Expedition
from Oodnadatta to Engoordina, by way of Dalhousie Springs on the out-journey,
and back by way of the River Stevenson, has been fully well explored for its
botany. And though every opportunity was availed of, yet only a very limited
number of species is worthy of note, some because new to the region (including
one, Threlkeldia proceriflora, previously unknown in South Australia), others

because reaching their most northern or southern limits in the meridional direction,

192 HORN EXPEDITION—BOTANY.

whilst a few are recorded because of their rarity. Some of the species have

already been mentioned as occurring in the Larapintine area.

The vegetation of this section of the country embraces that of the /food-ways
of the rivers and creeks, particularly the delta-like reticulation of the Stevenson
River north of Macumba, that of the savd-hil/s and that of the erbber-fields.

By far the richest flora as regards numbers of species is that found along the
margins of the water-channels at their lower elevations; here Eucalyptus micro-
theca, Acacia aneura, A. cyperophylla and A. homalophylla are conspicuous ; and in

favourable seasons a varied and luxuriant growth of grasses prevail.

The sand-hills yield a considerable variety of annuals after copious rain, but
Triodia is rarely present and only as 7. ¢vritans (when accurate determination was
possible), but Spznifex paradoxus is common.

However, the most prominent physiographic feature is that of the “ gibber-
fields,” which are most characteristically exhibited from near Macumba_ to
Charlotte Waters. The gibber-fields which are, probably, of the same nature as
the “stony desert” of Sturt, are co-extensive with the area in which the outcropping
surfaces of Cretaceous beds have been altered to a hard splintery rock by infiltra-
tion or by substitution of chalcedonic or opaline quartz. Where this kind of rock
occurs, usually as a crown to tabular elevations, the surface around is thickly
strewn with its broken fragments, ranging from blocks of several cubic feet to
road-metal size, and graduating to smaller dimensions with increasing distance
from the source of supply ; among the stones and beneath them is a red loess.
At some points could be recognised the sources whence the gzdders had been shed,
whilst more extensively the original stores have been exhausted. At the times of
our traverses, the g7bberfields offered the most desolate aspect—the annuals had
disappeared and the shrubby vegetation had been reduced to the condition of
skeletons of dried branches and twigs ; though, from traces of herbaceous plants,
it may not be unreasonable to infer that after copious rains an ephemeral vegeta-
tion may be comparatively abundant, it can never be absolutely abundant because
of the very limited space available by reason of the crowding of the gibbers.

Here follows a list of the plants observed around Mount Squire, twenty miles
north from Crown Point, the most northly extension of this type of country :—

Lepidium papillosum Helipterum Fitzgibboni
Frankenia levis Helipterum Tietkensi
Salsola kali Brachycome ciliaris

HORN EXPEDITION—BOTANY. 193

Bassia bicuspidata Eremophila Freelingi
Acacia aneura Hakea leucoptera
Acacia tetragonophylla Fimbristylis communis
Acacia Kempe Diplachne loliiformis
Cassia desolata Triodia sp.

Ptilotus incanus

A more typical collection is that afforded by the following list observed on
the tableland, about 700 feet elevation, at about five miles south from Charlotte
Waters, and also between Blood Creek and the Stevenson River :—A/riplex
rhagodioides, Salsola kali, Kochia aphylla, Eremophila Freelingt, Bassia diacantha ;
A. rhagodiotdes is the prevailing shrub, but where the stony surface gives place to
friable loam then AY affvia is dominant, where the surface is channelled by
water-runnels their courses are indicated by lines of the shrubs or small trees of
Acacia aneura, A. cyperophylla ov A. homalophylla and with them Cassia desolata.
Among bare patches of loam the following were noted :—Lepidium papillosui,
Frankenta levis, Euphorbia Drummondt, Boerhaavia diffusa, Ptilotus exaltatis,
P. incanus, Tragus racemosus, Cynodon ciliaris, Sporobolus actinoclados, Eleusine

cruciata, Aristida arenaria, Pappophorum commune and Astrebla pectinata.

2. List or Prants, New or Rare in tHe Recon.

[The asterisk pretixed indicates that the species is New for the Region. |
*Drosera Indica. Wet banks of the River Stevenson.

Hibiscus Krichauffi. Common from Oodnadatta to Crown Point.

Rumex erystallinus. River Stevenson between Oolabarrinna and Macumba.
*Atriplex elachophyllum., Crown Point and Adminga.
*Threlkeldia proceriflora, a hirsute variety. Adminga. New for South

Australia.

Kochia brachyptera. Adminga.
*Bassia salsuginosa. Adminga.

Crotalaria Mitchelli. Sandy loam-flats by the Stevenson River, from

Oolabarrinna to Macumba.

* Acacia homalophylla (giddea in the vernacular). Forms a dense scrub around
base of Mount Daniel; margining water-channels from Charlotte Waters to

Oodnadatta. Conspicuous by its ashy-grey foliage.

194 HORN EXPEDITION—BOTANY.

Tetragonia expansa. River Stevenson.

Loranthus grandibracteus. Parasitic on Lucalyptus microtheca, margining
water-channels from Oodnadatta to Ike’s Well on the Stevenson River; also Red
Mulga Creek near Dalhousie Springs.

Flaveria australasica. Giddea Creek near Oodnadatta.

Hyalolepis Rudalli. River Stevenson near Macumba.

Gnephosis arachnoidea. Crown Point, River Stevenson near Macumba.

Pepilidium Muelleri. River Stevenson near Macumba.

Bulbine semibarbata. Clay-pans about the Lower Stevenson River.
*Triglochin procera. Water-holes near Oodnadatta.

Panicum reversum. Finke River at Crown Point.

Anthistiria membranacea. Giddea Creek near Oodnadatta.

Eragrostis concinna et E. leptocarpa. By water-holes on the Lower Stevenson

River.

Poe PEN OX.

Notes on some Vegetable Baeudations.
By J. H. MAIDEN, F.L.S.

Professor Tate has placed in my hands for examination, the Vegetable
Exudations collected during the Horn Expedition. The samples were quite
small, and an exhaustive examination of most of them was therefore out of the
question, but they are of scientific interest, particularly in view of our scanty
knowledge of authentic substances of this character, especially from the interior of
the continent. The collection of such substances in the interior must necessarily
be a slow process, as the gums are washed off the trees by the first shower of rain,
the astringent exudations are affected both by the rain and by the fierce rays of
the sun which induce changes in their composition, while the resins readily dry up,

become brittle, fall to the ground and are lost.

No. 1. ‘Portion of an ant’s nest, consisting of sand agglutinated by gum
from Zriodia pungens, formed around the base of the grass, and continued as
cylinders around leaves and flower stalks. Tempe Downs.” This substance has
the appearance of a lump of reddish-brown clinker. When treated at a very low
temperature the resin melts (even in the flame of a match), and in its crude state
would make a useful cement. When the resin has burned away, the residue
consists of sand, principally quartz coated with ferric oxide, the latter being
removed by dilute hydrochloric acid. This ferric oxide assists to give the original
mass its reddish-brown appearance. When the original substance is treated with
alcohol (rectified spirit), the resin readily dissolves, leaving the sand, which differs
in no way from that obtained by burning off the resin. | Ether dissolves the
greater portion of the resin, but instead of the residual resin being dark brown as
in the case when alcohol is used, it is of a golden yellowish colour, and when
ignited burns away without residue, while that portion extracted by alcohol after

the ethereal extract has been removed, leaves a small quantity of residue.

The bright yellow resin melts at 83° C. The original resin extracted by
alcohol melts at 110° C., while the alcoholic residue left on removal of the resin
soluble in ether does not melt at 140° C. It consists partly of inorganic

mnmaterial. As ib was present in small quantities, its composition could not be

2oA

196 HORN EXPEDITION—BOTANY. APPENDIX.

determined in the small portion of material forwarded. The resin obtained
from Zyiodia irritans, R. Br. by ether, in appearance and colour resembles that
obtained from TZyiodia pungens, but it has a lower melting point, melting at
63° C. The brown resin obtained by alcohol, corresponding to that obtained
by alcohol from 7Z7iodia pungens, melts at 102° C. From the results of the
examination of the bodies contained in the resinous material of Zyéodia irritans 1*
it was suggested that the fat found was artificially introduced ; its presence would
lower the melting point of the resin. Judging from the appearance of the two
resins, their colour, odour, melting points, etc., there appears to be but little
difference in the resins obtained from Zriodia pungens and Triodia irritans, and

they may prove to be identical when prepared under similar conditions.

We have so few records of the finding of the Porcupine resin, that the following
is of interest :—‘‘Samples of resinous matter from roots of Spinifex, and tunnels
made by ants, found here for the first time, lying on the surface of the sandy
ground between bunches of Spinifex, apparently made of sand cemented with
some agglutinous secretion of the insect, or, what is more probable, the resinous
substance found at the roots of the Spinifex plant.” (W. T. Tietkens’ Exploration
of West Central Australia, in Trans. Roy. Geog. Soc. Vict., viil., 35).

No. 2. Gum of A¢alaya hemiglauca, F. v. M., Central Australia. Most of this
gum is quite colourless, and adherent to pieces of the wood of the tree, which belongs
to the natural order Sapindacez. A very small quantity only was received. It is
readily soluble in cold water, from which solution alcohol throws down a white
precipitate readily soluble in water but insoluble in alcohol, and resembling arabin
in its properties. It is pure gum and appears to differ little from the purest Gum
Arabic. A portion of the gum is also attached to a covering of the exterior of the
bore of a wood moth (probably a species of Cryptophasa) made of silken web, with
castings and debris attached. This gum would be a valuable article of commerce
if obtainable in quantity.

No. 3. Kino of Casuarina Decaisneana, ¥. v. M., near junction of Rivers Finke
and Palmer. The material, received 26th April, 1894, consisted of portions of the
tree coated with a dark brown resinous looking material which substance also filled
the hollows of the lumps. At places it had a varnishy appearance, but the greater
portion was a dull dry looking mass of an umbery colour. When powdered and
treated with water a reddish-brown solution is obtained, which consists principally

of a tannic acid giving a dirty purplish colour with ferric chloride and precipitable

* See a paper by me on “‘ Spinifex resin,” Proc. Linn. Soc. N.S.W., (2), vol. iv., p. 689, 1889. (A gum used by
the blacks for cementing the ends of spears and prepared from Spinifex roots). Collected at Napier Range, W.A.

HORN EXPEDITION—BOTANY. APPENDIX. 197

with gelatine and acetate of lead. With boiling water the solution is fairly clear,
but becomes turbid on cooling, from the presence of a body insoluble in cold water.
The material was too small in quantity to enable this body to be satisfactorily
determined. The residue left after treatment with water was partly soluble in
alcohol and consists of phlobaphenes insoluble in water but soluble in alcohol.
In alcohol the colour of the solution is much darker from solution of the
phlobaphenes. When this alcoholic solution is evaporated to dryness it has but
the slightest solubility in water, but is readily soluble in dilute ammonia from
which solution the phlobaphenes are precipitated on addition of acetic acid. — It is
one of those astringent exudations so common in Australia, usually designated
“inspissated sap.” A suflicient quantity of pure material is difficult to obtain,

and an exhaustive examination of it remains a desideratum.

No. 4. Roots of Leschenaultia divaricata, ¥. v. M., Central Australia, “Gum
extracted therefrom used by the aborigines as a cement.” [.Scevola depauperata and
Spintfex paradoxus are similar.| These roots consists of two parts —an inner very
tough woody portion consisting almost entirely of cellulose, and an outer tube which
readily slips off the inner string-like portion, This outer tube is covered externally
with fine sand, cemented into the material forming the basis of this outer covering.
The diameter over all is from 8 to 3 mm., the inner portion being 1 mm. When
treated with alcohol virtually nothing dissolves, the particles of sand not being
loosened in the least. When treated with water, but a very minute portion of a
gummy material dissolves ; this is precipitated by alcohol, is brittle when dry, and
readily soluble in water. No ordinary solvents dissolve the coating holding the
sand particles, these roots consisting almost entirely of cellulose and allied
substances, and it is not clear to me how, as stated, the aborigines extract a
material from the roots for cementing purposes. Further information upon this

point is certainly required,

No. 5. Flaky fibrous bark of Red Mulga, Acacia crperophylla, ¥. v. M.,
collected 9th May, 1894. Shrubby tree to thirty feet high, the red bark peeling
off in thin shavings. This specimen consists of very thin, flaky, fibrous portions
of the bark, and is very slightly astringent. The portion submitted evidently
consists of the external portion of the bark, and is similar in character to that
often found in dry country Acacia barks. The bark is not likely to be of
commercial value, and the portion received does not appear to be of special

scientific interest. It consists almost entirely of cellulose.

I desire to record my obligations to Mr. H. G. Smith, my assistant, for help

in the preparation of these notes.

ALPHABETICAL INDEX TQ PART lil—CEOLOGY AND BOTANY.

Abutilon, 141.
Acacian ba; N87, 193:
Acanthacez, 173.
Achyranthes, 146.
Actinoceras, 102.
Actinotus, 160.
Adhesive fruits, 130.
Adiantum, 186.
Adriana, 144.
ZEschynomene, 154.
Aizoon, 150.

Alfredi (Livistona), 180.
Alternanthera, 146.
Amadeus, Lake, 20,

Area of, 21.
Amarantacex, 146.
Amaryllidex, 179.
Ainmannia, 157.
Amphibolite, 91.
Andropogon, 183.
Angianthus, 166.
Anthistiria, 183, 194.
Anthobolus, 160.
Apocyne, 170.
arenarium (Endoceras), 101.
Aristida, 183.

Arkose, 83.

Artesian Bores, 62.

Arundo, 186.

Asaphus, 111.

Asclepiadew, 170.

Asperifoliz, 176.

Aspidium, 186.

Aster, 163.

Astrebla, 184.

Atalaya, 144, gum of, 196.

Atriplex, 148, 193.

Auriferous slate group, 114.

Australasian Genera of Plants,
Table of, with numbers of

species, 127.

australis (Bithinia), 73.

Ayers Rock, 8.

Ayersii (Helichrysum), 165.

Babbagia, 149.

Baeckea, 132, 158.

balonnensis (Melania), 73.
Bassia, 149, 193.

Bergia, 139.

Bidens, 167.

Bignoniacee, 173.
billingsiana (Palearea), 109.
Biotite, 78.

Bithinia, 73.

Boerhaavia, 151.

Botany, 117.

Brachiopoda (Ordovician), 110.
Brachycome, 162.
Brachychiton, 142.
Brachysema, 132, 134, 151.
Breweria, 171.

Brunonia, 168.

Buechnera, 172.

Bulbine, 194.

Burr-like Fruits, 129.

Burt Plain, 39.

Burtonia, 152.

Callitris, 133, 177.
Calocephalus, 166.

Calotis, 163.

Calycothrix, 158.
Campanulaceze, 168.
Candolleacex, 168.
Candollea, 168.

canescens (Swainsonia), 132, 133,

153.

Canthium, 162.

Capparide, 137.

Capparis, 137.

Capsella, 138.

Carissa, 170.

Caryophyllez, 146.

Cassia, 154.

Casuarina Decaisneana, Kino
196.

Casuarinee, 144.

Catosperma, 168.

Centipeda, 167.

Central Eremian Flora, 191.

of,

List of plants new or rare in

region, 193,
Centrolepis, 180.

HORN EXPEDITION—BOTANY. INDEX. 199

Cephalopoda (Ordovician), 98.
Chietites, 113.

Chambers Pillar, 7.

Chambersii (Brachyseina), 134, 151,
Chandler Range,

Elevation of, 6.
Cheilanthes, 186.
Chenopodium, 148.
chewingsi (Orthoceras), 100,
Chloris, 184.

Claypans, 22.

Claytonia, 146.

Clerodendron, 175.

Cleome, 137.

Codonocarpus, 151.

Comesperma, 139.

Commergonia, 142.

Commelina, 180.

Commelinee, 180,

Composite, 162.

Conglomerate (Post-Ordovician), 60,

Conifers, 177.

Conocardiun, 110.

Convolvulacex, 171.

Convolvulus, 171.

Corals (Ordovician), 113.

Corbicula, 73.

Corchorus, 143.

corrugata (Isoarca), 106.

Correlation of Larapintine (Ordo-
vician) Series, 115.

Corynotheca, 179.

Cowleana (Acacia), 187.

crassatelleeformis (Tsoarca), 107.

Crassulacex, 157.

Cretaceous plains, 7.

Cretaceous, Upper, 62.

Relation to Artesian Waters, 64.

Cretaceous, Supra, 65.
Crinum, 179.
Crotalaria, 152, 193.
Cruciferx, 138.
Crustacea, (Ordovician), 111.
Cryptandra, 159.
Ctenodonta, 105.
Cucumis, 162.
Cucurbitacere, 162.
Cuscuta, 171.
Cycade, 177.

Cynanchum, 170,

Cynoglossum, 176.

Cyperacere, 181.

Cyperus, 181.

Deemia, 170.

Daniel, Mount, Section of 63.

Danthonia, 184.

Datura, 172:

Daucus, 160.

Daviesia, 152.

Denudation, Factors of, 6.

Desert Sandstone, 65,

Paleontological features and
correlation of, 65,
Plants of, 67.

Diagnoses of New Species and
Genus of plants, 187.

dichotomalis (Orthis), 110.

Dicrastylis, 174.

Didiscus, 160, 188.

Dilleniacew, 137.

Diorite, 86, 87.

Diplachne, 185.

Diplopeltis, 145.

Diprotodon, 71.

Dodonea, 145.

Dolerite, 89.

Droseracexw, 139.

Drosera, 139, 193.

Duboisia, 172.

duponti (Orthoceras), 99.

Dysphania, 148.

eastii (Isoarca), 106.

Echinodermata (Ordovician), 113.

Economie Geology, 76.

Elacholoma, 172, 190.

Elatinew, 159.

Elatine, 139.

Eleusine, 184.

elevatuin (Orthoceras), 102.

Encephalartos, 177.

Enchyleena, 149.

Endeceras, 101.

Epacridew, 177.

Epaltes, 164.

Epidote, 91.

Eragrostis, 185, 194.

Erechtites, 167.

Eremian plants, Colonising power
and rapid germination of,

ToL,

200 HORN EXPEDITION—BOTANY. INDEX.

eremos (Scalites ?), 103.
Eremophila, 175.
Eriachne, 184.
Erianthus, 183.
Eriocaulez, 180.
Eriocaulon, 180,
Eriochlamys, 166.
Eriochloa, 182.
Eriostemon, 139.
Erodium, 140.
Erysimum, 138.
Erythriea, 170.
Erythrina, 154.
etheridgei (Isoarea), 105.
Kucalyptus, 158.
Kucyclus, 103.
Eunema, 102.
Kuomphaloid shells, 104.
Euomphalus, 105.
Euphorbiacee, 143.
Euphorbia, 143.
Euxolus, 148.
Evolvulus, 171.
Eyre, Lake, 19.
excentricum (Orthoceras) 102.
Exocarpus, 160.
Exotic Genera of Plants, Table of
and number of endemic and
exotic species, 124.
fasciguligerus (Cyperus umbellatus,
var.), 18.
Felspars, 84.
Ficoidea, 150.
Ficus, 144.
Filices, 186.
Fimbristylis, 181.
Finke River, 10, 11.
Ayea of Basin, 11.
Tributaries, 11.
Length and Rate of Fall, 13.
Nature of Channel, 14.
Flaveria, 194.
Fleshy fruits, 130.
Flora, Australian. Constituent
Elements of, 123.
Flora, Larapintine, 117, 124.
General conclusions with regard
io}, Ila ¥5)
Enumeration of Plants, 137.
Flora, Centra] Eremian, 191.

Fluviales, 180.
Fossil Deposits, Lacustrine, 73.
Frankeniacez, 145.
Frankenia, 145.
Frost, Influence of on Plants, 134.
Fruits, Burr-like, 129.
Adhesive, 130,
Fleshy, 130.
frumentacea (Acacia), 187.
Fuirena, 182.
Gabbro, 88.
Gaps, 18.
Garnets, 80.
Gastrolobium, 152, 134, 151.
Gastropoda (Ordovician), 102.
General Geology, 26.
Gentianex, 170.
George Gill Range, 5,
Geraniacesr, 140.
Gibbers, 24, 192.
Gillen, Mount, 5.
Gillenze (Didiscus), 188.
glaberrima (Hibbertia), 134.
glandulosa (Brachycome
var.), 162.
Glossogyne, 167.
Glycine, 154.
Gnaphalium, 164.
Gneiss, 92.
Gnephosis, 166, 194.
Gold, 76.
Gomphrena, 146.
Goodenia, 132, 169, 189.
Goodeniacez, 168.
Gordon River group, 114.
Gorges, 18.
Gossypium, 142.
Gramine, 182.
Grammitis, 186.
Gravels, River, 71.
grandiflorum (Gastrolobium), 132,
151.
Grevillea, 161.
Gum, of Atalaya, 196, of Leschen-
aultia, 197.
Gyroceras, 102.
gyrogonia (Murchisonia), 103.
Gyrostemon, 150.
Hakea, 161.

Halgania, 176,

ciliaris,

HORN EXPEDITION—BOTANY. INDEX.

Halorager, 157.
Haloragis, 157.
Hannafordia, 145.
Hart Range, 39.
headi (Pakearca), 109.
Heleocharis, 181.
Helichrysum, 165,
Heliotropium, 177.
Helipterum, 165.
Heterodendron, 145.
Hibbertia, 134, 137.
Hibiscus, 142, 193.

Horniana (Goodenia), 152, 169, 189,

Horni (Elacholoma), 172, 190.
Hyalolepis, 194.
Hyalostelia, 113.
Hybanthus, 138.
Hydrocharidew, 178.
Hydrocotyle, 159.
Hypericine, 139.
Hypericum, 139.
Hypostomes of Asaphus, 112.
ibex (Orthoceras), 99.
ibiciforme (Orthoceras), 99.
illarensis (Asaphus), 111.
Imperata, 183.
Indigofera, 152.
Tpomeea, 171.
irritans (Triodia), 185.
Tsoarca, 105.
Tsotoma, 168.
Tsotropis, 151.
Txiolena, 164.
James Range.

Physical Geography of, 5.

Elevation of, 6.
Jasmine, 170.
Jasminum, 170.
Johnston’s Range, 64.
Josephina, 177.
Juneacer, 180,
Juncus, 180.
Justicia, 175.
Kennedya, 154.
kinnekullense (Orthoceras), 100,

Kino of Casuarina Decaisneana, 196.

Kochia, 148, 193.

Krichauff Range, 12.
Labiatze, 173.

Lacustrine fossil deposits, 73.

Lamellibranchiata (Ordovician), 1

Lakes, 18.

larapinta (Hunema), 102.

Larapinta (Goodenia), 189.

larapinta (Pleurotomaria ?), 104.

larapintense (Orthoceras), 100,

Larapintine Flora, 117, 124.

Larapintine Region, 118.

Larapintine Series, Paleontolog
Literature of, 97,

Lavatera, 140.

Leguminosie, 151.

Lepidium, 138,

Leschenaultia, 168, gum of, 197.

Levi Range, 5.

Lilliacewe, 179.

Limosella, 172.

Lipocarpha, 182.

lissopeltis (Asaphus), 112.

201

OD,

ical

Literature Geological, References
Sb

to, 26.
Livistona, 132, 179.

Localities, fossil (Ordovician), 98.

Loranthacex, 160.
Loranthus, 160, 194
Lotus, 152.

Loudonia, 157.

Lowland vegetation, 119.
lutosa (Melania) 73,
Lycopodine, 186.
Lygodium, 186.
Lythrum, 157.

Macdonnelli (Macrozamia), 1:

178.

Macdonnelli (Encephalartos), 1
Macgregoria, 140,
Maerozamia, 154, 178.
Malvaceve, 140.
Malvastrum, I-41.
Mari (Livistona), 132, 179.
Marsdenia, 171.
Marsilea, 186.
Melaleuca, 158.
MeDonneil Ranges.

Physical Geography of, 3.

Height of, 4

Extent of, 3.
Melaleuca, 158.
Melania, 73.
Melhania, 142.

202 HORN EXPEDITION—BOTANY. INDEX.

Melothria, 162. Orthoceras, 98.
Mereenie Bluff, 59. Ottelia, 178.
Mica, 78. Oxalis, 140.
micans (Pteronites), 109. Palearca, 108.
Microcline, 84. Paleontology, 97.
microlineatum (Orthoceras), 99. Palme, 179.
Micro-pegmatite, 85. Pallimnarchus, 71.
Millotia, 166. Panicum, 182, 194.
Mimulus, 172. Papporophorum, 164.
Minuria, 162. Parietaria, 144.
Mirbelia, 151. Pedalinex, 177.
Missionary Plain, 5. Pennisetum, 182.
Mitchelli (Capparis), 137. pentagonalis (Kuomphalus), 105.
modioleformis (Isoarca eastil, var.), Pepilidium, 194.
106. Perotis, 183.
Modiolopsis, 109, Petalostylis, 155.
Mollugo, 150. Petrology, 82.
Mountains, 2. Phyllanthus, 143.
Muehlenbeckia, 150. Physical Geography, 1.
Muscovite, 78. Phytolaccew, 150.
Musgrave, Mount, 63. Pimelea, 151.
Myoporine, 175, Pittosporew, 138.
Myoporum, 176. Pittosporum, 138.
Myriocephalus, 166. Plagianthus, 141.
Myriophyllum, 158. Plagioclase, 84.
Myrtacez, 158. Plantagine, 170.
Naias, 180. Plantago, 170.
Neptunia, 155. Plectanthrus, 173.
Neurachne, 183. Pleurotomaria, 104.
Neweastlia, 174. Pluchea, 164.
Nicotiana, 172. Plumbagine, 145.
North Eremian Region, Plumbago, 145.
Botanical features of, 119. Podocoma, 164.
Nyctaginer, 151. Podolepis, 164.
Obsidian bombs, 70. pollens (Pallimnarchus), 71.
Olga, Mount, 9. Pollichia, 176.
Oldenlandia, 162. Polycarpa, 146.
Olivine, 89. Polygalez, 139.
Ophileta, 104. Polygala, 139.
opiformis (Isoarca), 108. Polygonacew, 150.
Opis, 108. Polygonum, 150.
orbicularis (Isoarea), 107. Polymeria, 171.
Ordovician system, 46. Pomax, 162.
Extent of, 51. Portulacez, 146.
Stratigraphical relations of, 52. Portulaca, 146.
Structural features of, 53. Post-Cretaceous Phenomena, 68.
Detailed sections of, 55. Post-Ordovician Conglomerate, 60.
Isolated portions of, 59. Potamogeton, 180.
Origin of Flora, 123. Pre-Cambrian System, 33.

Orthis, 110. Discussion on Age of, 37.

HORN EXPEDITION—BOTANY. INDEX.

Extent of, 39.
Junction of, with Lower
Silurian, 39.
Structural features of, 40.
Material Geology of, 41.
Primitive Australian Flora,
Representative Genera of, 131.
Primulacew, 170.
proceriflora (Threlkeldia), 137, 191.
Prostanthera, 173.
Proteacex, 161.
Psilotuin, 186.
Psoralea, 152.
Pterocaulon, 164.
Pterigeron, 164.
Pteronites, 109.
Ptilotus, 146.
Ptychosema, 155,
pungens (Triodia), 185, 195.
racemigera (Ipomea), 171.
Rainfall, 17, Diminution of, 1335.
Raphistoma, 103.
recticostatum (Trochoceras), 102.
ted Bank Gorge, 58.
Red Mulga, bark of, 197.
Reproduction of plants, Checks to,
133.
Restiacex, 180.
Rhagodia, 148.
Rhamnacewx, 159.
Rhizosperme, 186.
Rhynchosia, 154.
{iver Gravels, 71.
River Terraces, 72.
Rivers, 9.
robusta (Callitris), 133.
Rotala, 157.
Rubiacex, 162.
Ruellia, 173.
Rumex, 193.
Rutacee, 139.
Rutidosis, 166.
Salicariex, 157.
Salicornia, 149.
Salsola, 150.
Salsolacex, 148.
Samolus, 170.
Sandhills, 25.
Santalacewe, 160,
Santalum, 160.

Lo
co)
os

Sapindacew, 144.
Sarcostemma, 170.
saturni (Orthoceras), 102.
Saxatile Vegetation, 120.
Scevola, 168.

Sealites, 103.

Scirpus, 181.
Scrophularinew, 172.
Senecio, 167.

Seringea, 143.

Setaria, 182.

Sida, 141.

Siegesbeckia, 166,
Silicification, 68.
Solanacewe, 171,

Solanum, 171.

Sonchus, 167.
Spartothamnus, 174,
speciosum (Trochoceras), 102.
Spergularia, 146,
Spinifex, 183.

Spongida (Ordovician), 113.
Sporobolus, 184.
Sporadic occurrence of

Larapintine species, 132.
Stackhousia, 145.
Stackhousiew, 145.

Station Range,

Vegetation of, 121.
Stemodia, 172.
Stenopetaluin, 138.
Sterculiacexw, 142.

Stipa, 184.
Stirlingi, (Wedelia), 167, 188.
Stony plains, 25.
Straporollus, 103.
Strophomena, 111.
Styphelia, 177.
subleevigata (Corbicula), 73.
sulcata (Crassatella), 108.
Supra-Cretaccous, 65.
Swainsonia, 132, 153.
Table-lands, 7.
Table-topped Hills, 7.
tasmanicus (Straporollus), 103,
Tecoma, 173.
Templetonia, 152,
Tellinomya, 105,
Tephrosia, 153.
Terraces, River, 72.

206A

204 HORN EXPEDITION—BOTANY. INDEX.

Tertiary, 71. venustula (Melania), 73.
Tetragonia, 194. Vegetable Exudations, 195.
Teucrium, 174. Vegetation,

thorntoni (Asaphus), 111. Lowland, 119.
Thorntoni (Xanthorrheea), 132, 134, Saxatile, 120.

179; 191. Station Range, 121.
Threlkeldia, 137, 191, 193. Mount Gillen, 121.
Thryptomene, 158. Mount Squire, 192.
Thymelez, 151. Verbena, 174.

Thysanotus, 179. Verbeniacex, 174.

Tiliacea, 143. Vigna, 154.

Tillea, 157. Violaces, 138.

tortuosa (Paleearca), 109. Vittadinia, 163.

Tragus, 183. Wahlenbergia, 168.

Trema, 144. Waitzia, 164.

Trianthema, 150. Waltheria, 142.

Triraphis, 186. Water, absence of surface running,
Tribulus, 140. 14.

Triglochin, 180, 194. Waterholes, 15.

Trilobita (Ordovician), 111. Waterhouse Range, 5.
Triodia, 185. Elevation of, 6.
Triumfetta, 143. wattii (Isoarca), 108.
Trochoceras, 102. wattii (Palearca), 108.
truncatus (Modiolopsis), 109. Wedelia, 167, 188.

Typha, 180. Winnall’s Ridge, 60.
Typhacew, 180. Wurmbsea, 179.
Umbelliferse, 159. Xanthorrheea, 132, 134, 179, 191
Upper Cretaceous, 62. Xerotes, 132, 179.

Uralitic amphibolite, 91. Zaleya, 150.

Urticacer, 144. Zoantharia (Ordovician), 113.
Velleya, 169. Zygophyllez, 139.

Ventilago, 159. Zygophyllum, 139.

Printed by Forp & Son, 372 & 374 Drummond Street, Carlton, Melbourne.

TTT