Chapter II. it has been pointed out that the eroding agencies are not

actively in operation in our own day, and that there is good reason for the belief that the process of amalgamation by which Vanua Levu has been built up during a prolonged period of emergence, is not suspended at the present time. It is assumed that the uniformity in Nature’s methods has not been broken. If, however, we have here platforms of erosion, the coasts of Vanua Levu, as far as my interpretation goes, supply no evidence of it; and we have to imagine that a period of emergence extending over a geological age has been followed by a similarly vast period of erosion without much change in level.

Whatever agencies have been at work, the production of submarine platforms 10 to 20 miles in width must have been a stupendous operation; and we shall be obliged to inquire whether plateaux, either submarine or upheaved, occur in association with volcanic islands in other parts of the world, and under what conditions they have been formed. At least four hypotheses have been framed with regard to the submarine platforms of Fiji. There is first the original theory of subsidence of Darwin; but Vanua Levu, which presents one long story of emergence, offers nothing to support this view. There is the growth of a reef seaward on its own talus, as advanced by Murray. There is the theory of erosion of Agassiz. There is lastly my own idea of basaltic plateaux incrusted by reefs. We may therefore inquire as to the evidence afforded by Vanua Levu in favour of these views. Basaltic flows, in places covered by submarine deposits, form the low plains at its sea-border, where the platforms are broadest; and there rises a basaltic mountain of the Mauna Loa type, occupying most of the western end of the island. No one would be bold enough to place the limit of these basaltic flows at the water’s edge; and as is indicated in the sections, they probably extend for miles under the sea.

If we look for an island which in its extensive palagonite-formations, in its basaltic table-lands and later basaltic flows, in its huge mountain-ridges, and in its evidence of submergence, most resembles Vanua Levu, we seem to find it in Iceland. It is in Iceland, I think, that we must expect an explanation of many of the puzzling features in the structure of Vanua Levu.

I pass on now to refer to some of the general points in the geology of this island, which have been dealt with in detail in the earlier chapters of this work. With regard first to the distribution of the volcanic rocks, it may be remarked that my materials do not lend themselves to making a geological map. The most comprehensive idea of the principal points in the geological structure will be obtained by reading the description of the profile given in Chapter I. There is, however, a method in the distribution of the rocks that may be again noticed here. The plutonic rocks are very scantily exposed, as is shown on page 249; and they are not displayed at all in the western half of the island. The more basic eruptive rocks, the olivine-basalts and basaltic andesites, are mainly confined to the western half, that is, west of Nanduri on the north and of the Ndreke-ni-wai River on the south. Ordinary augite-andesites occur also in the western half; and together with the hypersthene-augite-andesites they are found over most of the rest of the island, excluding the north-east portion, east of Lambasa and Tawaki, where quartz-porphyries, oligoclase-trachytes, and acid pumice tuffs prevail. The acid andesites, including the hornblende-andesites and the dacites or felsitic andesites, are best represented in the Ndrandramea district in the midst of the basic rocks. They occur in the isolated peaks of Na Raro and Vatu Kaisia and in one or two other localities, as in the Valanga Range and on the shores of Natewa Bay in the vicinity of the Salt Lake. These peaks of acid andesites, as in the instances of Vatu Kaisia and Soloa Levu, are at times in part overwhelmed or surrounded by the basaltic flows. This singular feature of bosses of acid rocks in the midst of basaltic fields offers another point of resemblance between Iceland and Vanua Levu.

The mountain-types vary considerably, the ridge-mountains, however, being most characteristic of the island. The basaltic mountain of Seatura, though its lava-flows were evidently in the main submarine, belongs as before observed to the Mauna Loa type. In its radiating valleys and gorges and in other characters it recalls the description given by Dana of the island of Tahiti. The peaks of acid andesites, represented in the isolated hills and mountains of the Ndrandramea district, and in the solitary mountains of Vatu Kaisia and Na Raro, are the necks and stumps of submarine volcanoes dating back to the pre-basaltic period of the island. It is, however, in the great mountain-ridges of the central portion of the island, those of Va Lili, Korotini, Nawavi, Thambeyu, Mbatini, Mariko, &c., that we find, as just remarked, the most typical features of the internal topography of Vanua Levu.

Agglomerates overlying palagonite-tuffs and clays, that are usually foraminiferous and sometimes inclose molluscan shells, clothe the slopes of these mountain-ridges up to elevations of 2,500 feet and over above the sea. Most of these great ridges, now more or less covered over by these submarine deposits, represent lines of submerged vents, of which only a few raised their summits above the sea in the earliest stages in the history of the island. At this early period there were no coral reefs. Some of the ridges present a marked parallel arrangement, recalling the arrangement of the mountain-ridges and lesser chains of hills as described by Dr. Johnston-Lavis in the account of his visit to Iceland.[155] The description of Hekla (as given by Thoroddsen) as “an oblong ridge which has been fissured in the direction of its length and bears a row of craters along the fissure,”[156] comes very near to my conception of the original condition of these great mountain-ridges before the emergence. Dr. Johnston-Lavis sees in Hekla a type of volcanic mountain very different from that of Vesuvius and Etna. He regards it as a ridge marked by a number of parallel ridges and furrows, and built up along a main fissure with a number of subsidiary parallel fissures.

The part taken by palagonite in the composition of the finer deposits over the greater portion of Vanua Levu is another prominent characteristic of the island. Palagonite, as I have suggested in Chapter XXIV., is formed probably on the surface of submarine flows of an ophitic basaltic rock.

The age of the more recent of the deposits of this island, the fossiliferous tuffs, the pteropod-ooze rocks, and the foraminiferous muds, cannot be far different from that of the same deposits in other parts of the group, since it is apparent that the same general movement of emergence has affected both of the two larger islands. Professor Martin of Leyden informed Dr. Wichmann that the fossil shells found in the tuffs of Viti Levu, Ovalau, and other islands were Tertiary but not older than the Miocene.[157] Dr. Dall, after examining the fossil mollusks collected by Professor Agassiz from the elevated limestones of Fiji, confirmed the impression formed by the latter as to their late Tertiary age. None of the genera were extinct, and the fossils were in his opinion younger than Eocene and either Miocene or Pliocene.[158] The Rev. J. E. Tenison-Woods described as extinct Tertiary fossils, some corals and mollusks from the interior of Ovalau.[159] Mr. H. B. Brady, basing his conclusions on the character of the foraminifera, assigned a Post-Tertiary date to the Suva “soapstone” taken at elevations up to 100 feet in that neighbourhood.[160] Professor David referring to some fossil teeth of Carcharodon and to a fossil Tridacna found at Walu Bay infers that the deposits are at least as old as Pliocene but not as old as the earlier Tertiaries.[161] Since, as pointed out by Professor David, the latest movements of emergence have taken place in recent geological time, these various observations go to show that whilst the latest exposure of deposits has occurred in recent time the mass of the fossiliferous deposits date back to the Pliocene and the Miocene periods.

According to Wichmann these islands were in a continental condition during the Palæozoic and Mesozoic periods, and it was only in the later Tertiary age that the movement of subsidence began that prepared the way for the formation of the more recent deposits. The submergence during the Tertiary period and the subsequent emergence are facts that cannot be gainsaid; but we may ask where is the evidence of the continental condition during the earlier periods. There is little in the results obtained from Vanua Levu that directly supports such an hypothesis. Under such circumstances one ought to have discovered in the deposits of this island some evidence of this early condition, and there should be found in the fauna and flora some traces of the original organisms. According to Hedley there is some indication of a continental condition in the molluscan fauna, and he quotes Fairmaire as regarding the Coleoptera as of a continental character; but no one, that I am aware of, has found any direct evidence of the Pre-Tertiary periods in this group. It is in harmony with the geological characters to assume that these islands made their first appearance during the Tertiary epoch.

Coming to the subject of the movements whether of land or sea that led to the appearance of these islands, we shall not be begging the question if we speak of their “emergence.” There is no doubt as to there having been during and since the Tertiary epoch an emergence of some thousands of feet, allowing for the original depth of the foraminiferous deposits now found at elevations of over 2,000 feet above the sea. In Chapter II. it is shown that there is good ground for the belief that these changes of level have not altogether ceased. Of what nature, we may ask, is this movement. We have before us the grand conception of Suess that the emergence of the land in the different phases of geological time has been produced by the general lowering of the level of the ocean arising from local subsidences of the earth’s crust. This view in the case of the recent calcareous formations of the Pacific is applied to the terraces of the Loyalty Islands;[162] and it follows that it is also applicable to the elevated calcareous deposits of the islands of the Western Pacific as a whole, as in the case of the Tongan Islands, the New Hebrides, the Solomon Group, &c. Such a general change of level ought to be represented in the large island of Hawaii in the North Pacific, since it could not be confined to one locality in this ocean. There is no evidence of emergence, as far as I know, presented by this island. During my sojourn there, I examined much of its coasts. Now the antiquity of the flora of this group is sufficiently attested by the circumstance that it ranks first among the oceanic groups of the Pacific for the number of endemic plants that it possesses; and the same conclusions may be drawn from the insects and the birds. There is no evidence in this group, one of the most ancient of the Pacific archipelagoes, of that great movement of emergence, which is abundantly demonstrated over the Western Pacific.

The standpoint is therefore taken that the movement of emergence which began in the Tertiary period and is probably still in operation is confined to the southern portion of the tropical Pacific. Speaking of the time of the Fijian emergence, Professor Agassiz observes that “it is not unnatural to assume that it was coincident with the elevation of Northern Queensland, and that the area of elevation included New Guinea, the islands to the east of it as far as New Caledonia, and as far east as the most distant of the Paumotus, and extended northward of that line to include the Gilbert, Ellice, Marshall, and Caroline Islands.”[163]

From the report of Mr. Andrews[164] it is evident that in the Lau Islands of the Fiji Group volcanic outbreaks have taken place since the last upheaval. He describes in the case of Mango and other islands the manner in which cliffs of limestone form inliers in flows of andesitic lava. In the history of these islands he first distinguishes the period of calcareous deposits, when the bedded limestones forming the submarine plateau were laid down. Then followed a period of volcanism during which masses of volcanic materials were erupted along the axis of elevation. Alternating epochs of upheaval and stable equilibrium ensued, during the last of which the reefs grew outwards and formed the terraces now so characteristic of the profiles of the islands. After the last upheaval the volcanic forces became again active. There is much of special interest in the account given by Mr. Andrews of the Lau Group. The blocks of limestone included in the volcanic agglomerates distinguish the Lau detrital rocks from those of Vanua Levu. There is no evidence that coral reefs existed during the early stages of the emergence of Vanua Levu to be obtained from the submarine formations found on the higher levels, 1,000 to 2,500 feet above the sea.

The period of emergence for this island may be divided into an earlier and into a later stage, the last corresponding to the age of emergence of the Lau Islands. The earlier stage, which may be termed the “Pre-Lau” stage, is represented by the deposits of the higher slopes of Vanua Levu, that is above 1,000 or 1,200 feet. This is really the critical epoch in the history of this group, and assuming that the movement of emergence has been fairly uniform over the archipelago we cannot but be astonished at the absence of all traces of ancient reefs in the earlier stage.

We may infer from the observations of Mr. Lister[165] that the islands of the Tonga Group represent the Lau stage of the emergence. They are similar in height and in general geological structure to the islands of Lau, that of Eua, for instance, which has an elevation of 1,100 feet, being formed of reef-limestones overlying volcanic tuffs. Dykes penetrate the tuffs but do not enter the incrusting calcareous strata. Mr. Harker,[166] after examining the collections of Mr. Lister, remarks that all the rocks excepting those from Falcon Island appear to be of submarine formation. The volcanic material, he adds, seems to have been almost exclusively of fragmental character. It would be rash, it is remarked, to refer all the rocks to a Recent age, and some of them may be found to go back far into Tertiary times.

My division of the long period occupied by the emergence of the Fiji Islands into two stages, the Lau stage corresponding to elevations of less than 1,000 or 1,200 feet, and the Pre-Lau stage which includes the earlier evidence of emergence found at heights exceeding these elevations and ranging up to 2,000 or 3,000 feet, may perhaps be applicable to other regions of emergence.

As bearing on the question of the isolation and antiquity of the Pacific Islands the following approximate results for the Hawaiian, Fijian, and Tongan floras may be here quoted.[167] These data are liable to correction; but they are near enough to the truth to be very suggestive. Of peculiar genera of flowering plants and ferns the Hawaiian Islands possess about 40, the Fiji Group about 16, and the Tongan Islands none. Of endemic species of flowering plants there are about 80 per cent. in Hawaii, about 50 per cent. in Fiji, and 3 or 4 per cent. in Tonga. Granting that there is much to be done yet in the investigation of these floras, it would be underrating the brilliant results of the labours of Hillebrand and Seemann to characterise their work as sampling. Let us suppose, however, that the floras of Hawaii, Fiji, and Tonga have been only sampled, the data above given would be still reliable. It is quite possible to obtain a botanical equivalent corresponding to the geological estimates of the relative ages of these islands; and taking the proportion of endemic plants as our guide, the Lau stage, as represented by the Tongan Islands, would have a value of 3 or 4, the Pre-Lau stage now exhibited in the earliest stage of emergence of Vanua Levu would have a value of 50, and the Hawaiian stage older than all would have a value of 80. These results are intended as suggestive and I hope to work out this subject in the second volume. They make the problem of the relative antiquity of these islands more mysterious than it even appeared before.

With regard to the vexed question of the light thrown on the past condition of these islands by the present state of their floras and faunas, it may be at once observed that my belief in the general principle that islands have always been islands has not been shaken by the results of the examination of the geological structure of Vanua Levu. In a correspondence in _Nature_ about fifteen years ago it was suggested by me that this is the position we ought to take with regard to the stocking with plants of the islands of the Southern Ocean, such as Kerguelen; and I take the same standpoint for the islands of the Pacific. If the distribution of a particular group of plants or animals does not seem to accord with the present arrangement of the land, it is by far the safest plan, even after exhausting all likely modes of explanation, not to invoke the intervention of geographical changes. New possibilities of inter-communication, new ways of looking at old facts, and new discoveries of an unexpected nature come monthly before us in the progress of scientific research; and I scarcely think that our knowledge of any one group of organisms is ever sufficiently precise to justify a recourse to hypothetical alterations in the present relations of land and sea.

The hypothesis of a Pacific continent,[168] whether it takes a trans-oceanic form, as advocated by Von Ihering, Hutton, Baur and others, or whether it is represented by an island-continent isolated in mesozoic times, as suggested by Pilsbry, receives no support from the geological characters of Vanua Levu. Nor can I accept as regards Fiji Mr. Hedley’s theory of the Melanesian Plateau. There is no evidence that the various islands of the Fiji Group were ever amalgamated and no indication of a geological nature that they were ever joined to the Solomon Group. The Fijis, as we see them, have had an independent history, and the process at work is not one of disruption but of amalgamation, lesser islands being united to larger islands during the prolonged period of emergence. Mr. Hedley, however, has some weighty data on his side more especially zoological; but even here it would be wise to suspend one’s judgment. Though the great mass of botanical evidence is as respects Fiji opposed to such connections, the distribution of Dammara may, however, be fairly claimed on their behalf.

The dilemma into which such discussions lead us is aptly stated by Dr. Pilsbry. If we do not accept the hypothesis of a Pacific continent, we have to explain the cessation of the means of transportal in later geological times, since this is implied in the isolation necessary for the development of peculiar characters in a fauna or a flora. This was the dilemma that presented itself to me in studying the origin of the Fijian plants. Assuming on geological grounds that the insular condition had been always maintained I had to explain the differentiation in the inland plants, or in other words to account for the failure of the means of transportal that once existed. Since this subject bears directly on the past condition of the Fiji Islands, I may be pardoned for referring to it here. It belongs properly to the second volume which it is proposed to devote to the dispersal and distribution of Pacific plants; but as I contest the pre-existence of a Pacific continent, it is fitting though not necessary that this difficulty should be faced at once.

If we in imagination combine in a typical island the characters of the flora presented by islands of different elevation in the Pacific we get a result of this kind in an island of the height of Hawaii, nearly 14,000 feet. The littoral plants of such an island are found all over the coasts of the tropical Pacific, and for the explanation of this fact we look mainly to the agency of the ocean-currents. The plants of the mountain summit, belonging to the temperate genera of Geranium, Rubus, Ranunculus, Vaccinium, &c., are represented at least generically on the tops of the lofty ranges of the Pacific coasts and in the interior of the continents; and we find the explanation of the wide diffusion of such plants in the agency of the migrant birds that at no distant time, if not actually in our own time, were regular visitors to these mountain regions. The plants of the marsh, of the stream, and of the pond, belong often to species that occur in similar stations over a great portion of the world, such as species of Drosera, Ruppia, Potamogeton, &c.; and here the agency of wild duck and other waterfowl may be observed in active operation.

But when in such an island we regard the intermediate region between the uplands and the coast, usually the forest-zone, we find an area of change not only for the plants but also for the birds. It is here that the new genera of plants have been developed that distinguish the floras of the Pacific groups each from the others; and here also the migrant bird, having from some cause changed its ways, has given rise to new varieties and to new species. It is with this loss of the migratory powers of the birds of the forest-zone that I connect many of the important differences between the forest-floras of the different groups of the Pacific. At one time, it would seem, birds were far more active agents in dispersing seeds and fruits over these archipelagoes than they are at present; but it is not held that this is concerned with the extermination and extinction of the birds of these islands in the present day. The change dates far back and is far-reaching in its effects. It is assumed in this argument that the alpine plant and the plant of the pond and of the sea-shore preserve their characters by reason of the means of free dispersal that they still enjoy; and it is inferred that the plant of the forest-zone has varied more because opportunities of transportal of its kind no longer are afforded. Many a line of ancient migration is now broken.

It is suggested that in the past when birds were more generalised in type they were much more migratory in habits and that limitation of range has been associated with specialisation. The plants dispersed by the birds have undergone a parallel series of changes. At first widely distributed, as in the more generalised types of birds, they became localised in proportion as the birds to which they owed their means of dispersal lost their migratory ways; and both plant and bird began to vary. There is, I am convinced, a profound connection between birds and plants, of which we now perceive only the last of a long series of changes. This subject will be dealt with at length in the volume on plant-dispersal; and it is only referred to here to illustrate my contention that we have yet much to learn before it would be safe to look to hypothetical changes of sea and land to explain difficulties in distribution.

APPENDIX

_Note on the Stone-Axes._—Two of these polished stone-axes from a collection made in Vanua Levu were selected for sections. One is light-green and smooth. The other has a very different appearance, being blackish and rather rough, its smooth surface having been apparently lost by lying in a stream-course or in wet ground for a long period. Both, however, are made of the same type of basaltic rock, the specific gravity in one case being 2·93, in the other 2·97. It is an aphanitic basalt with scanty olivine containing little or no residual glass and referred to genus 40 of the olivine-basalts. It is by no means a common type of basalt in Vanua Levu, and I cannot refer it to any particular locality on account of the peculiarities it presents when contrasted with rocks of the same genus. The olivine is very scanty and small, and in one of the specimens is represented only by pseudomorphs. The felspar-lathes vary usually from ·05 to ·2 mm. in length, and the augite granules which are very abundant are ·01 or ·02 mm. in diameter. There is an occasional small phenocryst of augite. The rock shows little or no alteration and cannot be characterised as a greenstone. The greenish hue of one axe is due to weathering; but its extension into the internal black portion of the tool is not appreciable.

* * * * *

_Note on the ascent of the tide up the Ndreketi River._—On July 20th and 21st, 1899, by observing the surface density it was ascertained that at high-water the sea-water reached Navundi a mile or two below Mbatiri. At low-tide it reached about half-way between Kanathangi and Navundi. The moon was in her quarters.

* * * * *

_Note on the “talasinga” districts._—This subject will be discussed in the second volume.

INDEX

NOTE.—It has been deemed best to follow the example of the Admiralty surveys in the spelling of native names. In this book, therefore—

Mb = the Fijian B Th = the Fijian C ND = the Fijian D NG = the Fijian G and Q

Abbreviations, for rock descriptions, 236

Acicastello, Sicily, basalt and palagonite, 347

Acid and basic rocks, regions of, 219, 374

Agassiz, Prof. A., 294, 373, 376, 377

Agates, 138, 139, 227, 353, 354

Agglomerates; _see_ Volcanic agglomerates

Algæ in hot springs, 24, 25, 33, 38

Alps, magnetic rocks of the, 362, 363

Altered rocks; _see_ Propylites, etc.

Andesites, acid, 98-108, 112, 123-127, 193, 194; relative frequency of, 235; classification of, 293-306; distribution of, 374; peaks in basaltic flows, 104, 115, 116, 374; altered, 105, 297; columnar, 102, 104; pre-basaltic, 375

Andrews, Mr. E. C., 7, 22, 294, 350, 378

Artesian reservoirs, 39

Augite, crystals of, in tuffs, 45, 182, 193

Augite-andesites, 51, 162, 199, 204, 209, 232, 235, 294, etc.; classification of, 239, 245, 246, 266-284; distribution of, 374; aphanitic, 117-120, 125, 162, 168, 279; relative frequency of, 235; _see_ Basaltic andesites

Avuka, range, 179

Axes, stone, structure of, 383

Bare-poll, peak, near Soni-soni, 93

Barrack, Mr. A. H., 27, 123

Barrack, Mr. Alex., 364

Barratt, Mr., 68

Barrier-reef, great, of Fiji; _see_ under Submarine plateau

[169]Basaltic andesites, 47, 56, 64, 75, 108, 123, 137, 147, 148, 160, 164, 190, 204, 206, 208, 288; classification of, 239, 266, 278; distribution of, 374

Basaltic rocks, extensive disintegration of, 57, 64, 72, 129

Basaltic flows surrounding hills of acid andesite, 104, 115, 116, 374

Basaltic plains and plateaux, 6, 55, 62, 82, 107, 128-135, 373

Basaltic submarine flows, 338, 342, 344, 346, 347, 372, 375; _see_ under Submarine plateau and Basaltic plains

Basalts, columnar, 3, 63, 78, 83, 84, 85, 123, 129, 133, 147, 170, 173, 203, 260, 284

Basalts, ophitic, 50, 74, 114, 133, 137, 138, 155, 159, 162, 191, 204, 213, 252, 256, 347; the ophitic habit, 237, 238; ophitic sub-orders, 236, 241-245; ophitic genera, 256, 262, 272-276, 283

Basalts, olivine, relation of black and grey, 89, 90; classification of, 239, 241-244, 252-265; relative frequency of, 235; distribution of, 374

Basalts, grey olivine, 65-67, 73-75, 77, 89, 253-255, 257, 261, 263

Basalts, highly basic, 258

Basalts, of Acicastello, 347; of Mbua and Ndama plains, 58, 134, 262, 278; of Ndreketi plains, 133, 134; of Sarawanga plains, 129, 134, 262; of Savu-savu peninsula, 190, 288; of Seatura, 63-72, 85; of Solevu Bay, 75-77; of Wainunu, 85; of Ulu-i-ndali, 89

Basalts associated with palagonite, 347

Basic glass, 312, 338; _see_ Pitchstone, Crush-tuffs, Hyalomelan-tuffs

Bastite, 182, 297

Baur, Mr., 380

Blyth, Mr., 123

Brady, Mr. H. B., 322, 376

Breccias; _see_ Volcanic agglomerates

Bronzite, 182

Bromlow, Dr., 29

Büchner, Dr. Max, 22

Bulling, Mr., 32, 36, 232

Bunsen, on palagonite, 343, 344

Carbonate of iron, concretions of, 227, 351, 356

Carcharodon, 376

Chalcedony, 13, 138, 162, 183, 199, 226-22, 350-355; _see_ Agate, Onyx, Flints

Chalmers, Mr., 233

Charts, old and new compared, 18, 19

Chert, 355

Classification of volcanic rocks, 235

Coleoptera of Fiji, 377

Columnar structure; _see_ Basalt, Acid andesite, Dacite, Oligoclase-trachyte

Combe, Commander, 15

Cooper, Mr. H. S., 29

Coral reefs, upheaved, 7-12, 189, 200, 201, 318; their absence in the higher levels, 7, 8, 12, 19, 375

Craters, traces of, 44, 52, 67, 80, 166, 186, 192, 195, 202

Crush-tuffs, 55, 94, 149, 157, 341; general description, 334; _see_ below

Crushing of basic glass; in veins, 340, 341; on surface of a submarine flow, 93, 338; in matrix of pitchstone-agglomerate and in rubbly pitchstone, 94, 142, 145, 157, 313; its connection with palagonite, 93, 339, 340-342, 346

Cumming, Miss Gordon, 22, 25, 29

Dacites, 3, 5, 100, 108, 235, 294, 304; columnar, 101, 102; definition of the term, 295; classification and characters, 240, 302; _see_ Acid andesites

Dall, Dr., 376

Dana, Prof., 3, 10, 11, 16, 21, 26, 72, 84, 129, 135, 218, 309, 363

Darwin, Mr., on barrier-reefs, 373

Datum-mark, 195

David, Prof., 376

Deep-sea deposits, 337

Delanasau, 68

Dillon’s Rock, 45

Diorite, 182, 193, 235, 249, 251

Doelter, on hornblende paramorphism, 308

Doleritic, use and definition of the term, 236, 238, 259, 274

Dolomite, 7

Drayton, peak; _see_ Mariko

Dykes, 51, 54, 63, 68-72, 78, 81, 142, 144, 148, 155, 156, 163, 164, 170, 171, 184, 199, 202, 209, 216, 220, 233, 234, 267, 268, 270, 277, 280, 282; their two sets of felspar-lathes, 238

Eakle, Mr., 293, 294

Earthquakes, 37

Emergence of Vanua Levu, 1, 7-20, 321, 376-379; age of, 376

Etna, mount, coast springs of, 39; dykes in Valle del Bove, 237; magnetic bomb, 364

Fairmaire, M., 377

Faro, island, Solomon Group, 2

Fawn, harbour, 9, 200, 318

Felsitic andesites, 106, 108, 295, 300; _see_ Acid andesites and Dacites

Felsitic groundmass, as employed in classification, 236, 239, 240, 249

Felsitic orders, 249, 291, 297, 300, 302

Felspar-lathes in classification, 236, 241

Fern, tree, silicified caudex of, 360

Fish-scales, fossil, 154

Flints, 13, 81, 83, 138, 139, 222, 226, 350-360

Floating islands, 225

Floras of Fiji, Hawaii, and Tonga, 379

Flow-arrangement in classification, 236-238

Folgheraiter, Dr., 362, 365

Foraminiferal limestones, 130-132, 202, 318

Foraminiferous deposits (tuffs, muds, clays), 96, 109, 130, 134, 136, 139, 149, 154, 161, 170, 198, 205; description of, 321-333; altered, 324-326; thickness of, 156; _see_ Globigerina deposits and Palagonite-tuffs

Fossilised trees, 233

Freeland, Mount, 2, 6, 203-206, 269, 274

Gabbros, 180, 182, 184, 211, 235; classification of, 239, 240; characters, 249, 250; _see_ Plutonic rocks

Geikie, Sir A., 375

Giant sedge; _see_ Scirpodendron

Globigerina deposits, 10, 55, 131, 158, 177, 187, 189, 190, 221, 321-326, 344; _see_ Foraminiferous deposits

Globigerina limestone, 319

Gold, alluvial, in Vanua Levu, 116

Granular pyroxene, the sub-orders characterised by, 236, 241, &c.

Greenstones; _see_ Propylites

Groundmass, characters of, used in classification, 236-238

Haig, Major, on magnetic rocks, 363

Hale Peak, 210, 212

Hanusz, on floating islands, 226

Harker, Mr., 362, 367, 379

Harman’s Point, 191

Hawaii, 2, 38, 85, 363; flora of, 379; coast springs of, 38

Hedley, Mr., 376, 380

Hekla, Mount, 375

Holmes, Mr., 68

Hornblende, magmatic paramorphism of, 293, 299, 301, 303; process described, 306

Hornblende-andesites, 91, 184, 193, 194, 201, 235, 294; _see_ Acid andesites and hornblende-hypersthene andesites

Hornblende-gabbro, 184, 249, 250

Hornblende-hypersthene-andesites, 240, 298-302

Horne, Mr., 10, 21, 22, 25, 34, 55, 141, 143, 194, 195, 203, 225; _see_ the preface

Hornstone, 350

Hot springs, general description of, 21-42; list of, 40; analysis, 28; distribution in Vanua Levu, 36, 138, 233

Humboldt, A. von, on magnetic rocks, 361, 365

Hussak, on magmatic paramorphism, 308

Hutton, 380

Hyalomelan tuffs, 47, 80, 110, 333, 334

Hydrothermal metamorphism; _see_ Solfataric

Hypersthene; _see_ Pyroxene, rhombic

Hypersthene-andesites, 294, 296

Hypersthene-augite-andesites, 5, 52 147, 161, 164, 168, 171, 173-175, 178, 179, 182, 186, 190, 199, 201, 203, 208, 211, 230; classification, 240, 247, 248; characters of the orders and sub-orders, 285-292; relative frequency, 235; distribution, 374

Iceland, Vanua Levu compared to, 374, 375

Iddings, Mr., 306

Iron ore; _see_ Limonite

Iron sand, magnetic, 83, 106, 357

Ironstone gravel, 356

Islands, permanence of, 380, 381

Jackson, Dr. C. T., 28

Jasper, 13, 121, 139, 199, 350, 351, 355

Johnston-Lavis, Dr., 347, 375

Kalakala, Mount, 103, 305

Kalikoso District, 10, 15, 224-228, 350, 356, 358

Kandavu, 293, 306; hot springs of, 22

Kavula, 65, 66

Kia Island, 2

Kioa Island, 2

Kiombo Coast, 92

Kleinschmidt, 22, 25, 293, 350

Koro, significance as a prefix; _see_ Place-Names

Koro-i-rea Hill, 75, 77

Korolevu Hill, 45; natural section near, 48

Korolevu River, 62, 64

Koroma, Mount, 3, 51, 285

Koro-mbasanga Mountain, 166-169, 289; name wrongly applied in Admiralty charts, 5, 172

Koro-navuta, 135

Koro-ni-valu; _see_ under Towns

Koro-ni-yalewa Mountain, 117

Koro-tambu Mountain, 167, 171

Korotasere, 208

Korotini Bluff, 156

Korotini Range or Tableland, 5, 153-165, 167, 325

Koro-utari, 163

Koro-wiri, 139

Kumbulau Peninsula, 90-95

Kuru-kuru District, 228

Lambasa coast, 218

Lambasa Plains, 138, 351

Lambasa River, 15, 138

Landslips, effects of, 111, 178, 327

Langa-langa River, 220, 225

Lango-lango River, 122

Lau Group, 7, 294, 378

Lava-flows, indications of sub-aerial, 52, 71, 119, 133, 152, 187, 190, 213, 232

Lea District, 199

Lekumbi Point, 12, 19, 60

Lekutu District, coast of, 11, 50, 273; plains, 128, 351, 353, 356; promontory, 16, 18; river, 18, 62, 65

Limestones, recrystallisation of, 131; coral, 318; _see_ Foraminiferal limestones

Limonite, deposits of, 56, 132, 138, 226, 228, 351, 352, 356, 359

Lister, Mr., 378

Liversidge, Prof., 29

Liwa-liwa, 119

Loma-loma Ridge, 141

Lovo Valley, 169-173

Lovutu, 156

Macdonald, Dr., 21

Magma lakelets, 47, 71, 92, 273, 276, 277; description of, 339-342, 346, 347

Magmatic paramorphism; _see_ Hornblende

Magnetic iron sand, 83, 106, 357

Magnetic peaks and rocks, 77, 108, 174, 186, 361-371

Mako-mako Hill, 103

Mali Island, 2, 218

Mali Point, 218

Malolo Island, 294

Mangrove belt, bare tracts in, 11, 14; relation to reef-flat, 13; rate of growth, 15, 19

Mangrove islands, growth of, 16, 17

Mariko, range and peak of, 5, 173, 185-189, 289, 368

Martin, Prof., of Leyden, 376

Masusu District, 84

Mauna Kea, 2

Mauna Loa, 2, 3, 363

Mauritius, magnetic rocks of, 363

Mbale-mbale District, 143, 313; river, 150

Mbatini Mountain, 5, 166, 172-174, 367

Mbati-ni-kama, hot springs of, 33

Mbatiri, 134, 324

Mbenutha Cliffs, 109-111, 323

Mbona-lailai Mountain, 101

Mbua District, 3, 36, 37, 47; bay, 18; coast, 12

Mbua and Ndama Plains, 55-58, 356

Mbua-Lekutu Divide, 55, 297

Mbua shell-bed, 12, 58

Mbuthai-sau Valley, 218, 219

Mbutu-mbutu River, 79, 279

Middle Point, 137

Mountain ridges and their structure; _see_ under Ridge-mountains

Mountain-towns; _see_ Towns

Muanaira, 198

Mumu Peak, 108-110

Murray, Sir J., 337, 373

Naikovu Rock, 364

Nailotha Mountain, 6, 214-216, 310

Naindi Bay, 8, 189, 191, 195, 318

Naindi Gap, 189, 192

Naithekoro, 190

Naithombothombo, point, 54; range, 229

Naivaka, 2, 3, 11, 18, 43-45, 261

Na-kalou, 133

Na Kama, Savu-savu, 25; Lambasa, 32

Nakambuta District, 148-150

Nakarambo, 208

Na Kula, valley, 184; range, 230

Nambuna District, 106

Nambuni Spur, 144

Nambuonu, hot springs, 32

Nandi Bay, 78

Nandi Gorge, 69, 78, 278

Nandongo, island, 16, 17; town, 216; hot springs, 33

Nandronandranu district, 117-121

Nandroro District, 66

Nandua District, 86, 320, 344

Nanduri District, 11, 14, 135, 136

Nangara-ravi Cave, 141

Nangara-vutu, 205

Nangorongoro Peak; _see_ Ngaingai

Na Raro Gap, 127

Na Raro Mountain, 2, 5, 123-127, 296, 301, 305

Narawai District, 66

Nareilangi, 124

Narengali District, 140, 147, 149

Narikosa Point, 220

Na Salia, 151

Na Savu, tableland, 79-81; falls, 79, 279

Na Seyanga, 108

Na Sinu, 146

Na Suva Range, 64

Na Suva-suva Hill, 192, 369

Natasa Bay, 209

Natewa Bay, north-coast, 9, 208, 209, 291

Natewa Peninsula, 6, 9, 197-206

Nativi, 50

Natoarau, hot springs, 23; river, 158

Na Tokalau, 91

Natoto Hill, 229

Natua District, 134, 149, 323

Natuvo or Natuvu, hot springs, 33, 209

Naumann on polaric lavas, 364

Navakaravi Hot Springs, 34

Navakavura, 96

Na Vatu Islet, 94

Navetau, 205

Naviavia Islet, 8

Navingiri, 46

Navuni, 202; hot springs, 35

Navuningumu, 108-112, 303, 368

Nawavi, range, 135; hot springs near, 31

Nawi or Na Wi, island, 26, 192; hamlet, 211

Ndaku-ndaku, bay, 208; hot springs, 34

Ndama, river and valley, 62, 67, 68, 71; plains, 55-58

Ndavutu, district and river, 87; for hot springs; _see_ Wainunu

Ndawathumi, 64, 80

Ndevo district, 205; hot springs, 35

Ndoendamu Mountain, 209, 212

Ndrandramea, district, 2, 3, 83, 296; map, 99; description, 98-112

Ndrandramea Mount, 102, 296, 300, 304, 368

Ndranimako, 96, 322, 351

Ndrawa, district, 120, 281; river, 118, 120

Ndreke-ni-wai, Natewa Bay, 200, 203; hot springs, 34

Ndreke-ni-wai, Savu-savu Bay, 150, 152

Ndreketi, river, 15, 128, 132, 383; plains, 132, 273, 351

Ndriti Basin, 67-72, 268, 270, 282

Ndrukau Mountain, 213

New Hebrides, 1

Ngaingai Mountain, 100, 296, 302, 304, 368

Ngala Mountain; _see_ Freeland

Ngalau-levu Range, 6, 199, 200, 370

Ngangaturuturu Cliffs, 119

Ngau Island, hot springs of, 22

Ngawa River, 138

Ngelemumu, 180, 219

Ngone Hill, 183

Nukumbolo, district, 151, 161, 162; hot springs, 24

Nukunase or Nuku-ngase, 50, 270

Nukumbalavu, 190

Nuku-ndamu, 232

Numbu, 227

Numbu-ni-a-vula, 176

Oddone on magnetic rocks, 362

Oligoclase-trachytes, 6, 207, 219, 229; description of, 308; distribution, 374; altered, 214-216; columnar, 215, 220, 230, 231, 233

Olivine rocks, classification of, 239

Olivine-basalts; _see_ Basalts, olivine

Ono Island, hot springs, 22; acid andesite, 293; flints, 350

Onyx, 139, 227, 228, 353

Opal, 162, 163, 183, 351, 353

Ophitic basalts, their relation to palagonite, 347

Ophitic structure, as used in classification, 236, 237, 238

Ophitic sub-orders and genera, synopsis of, 241-248; description of, 256, 272-276, 283

Orthophyric groundmass, as used in classification, 236, 237, 239, 240

Orthophyric orders and genera, 248, 290, 296, 297, 299

Ovalau, 294, 350

Palagonite, chapter on, 337-349; _see_ also Palagonite-tuffs, Crush-tuffs, Crushing of basic glass, Pitchstone &c.

Palagonite of Acicastello, 347

Palagonite tuffs, classification and characters, 317-336; zeolitic, 334; marls, 335, 344; modes of occurrence, 5, 48, 53, 80, 81, 95, 96, 117, 118-122, 130, 131, 141, 143, 145, 148, 156-161, 169, 177, 193, 198, 202, 213

Palagonite, hydration and degradation of, 329, 348

Phenocrysts, their use in classification, 236

Pickering, Mr., 35

Pieper, Dr. O., 28

Pilsbry, Dr., 380

Pitchstone agglomerates and rubbly pitchstones, petrological characters, 312, 313; evidence of crushing and its connection with palagonite, 92-94, 142, 145, 157, 312, 313, 334, 340-342, 346 (_see_ Palagonite, Crush-tuffs, Crushing of basic glass); mode of occurrence, 105, 108, 142, 157, 169, 229, 230, 309

[170]Place-names, meaning of Fijian, 75, 79, 102, 119, 151, 172

Platania, Prof., 119, 347

Plutonic rocks, general description, 249-251; relative frequency, 235; distribution, 249, 374; mode of occurrence, 180, 182, 184, 185, 193, 211

Polarity of magnetic rocks, 366-370

Porphyrites, 136, 175, 181, 197, 199, 204, 211, 261, 268, 274, 299; belong to many orders, 236

Prismatic pyroxene of groundmass, its use in classification, 236, 241-248; sub-orders and genera, 265, 270-272, 283, 287, 289, 298, 300, 302

Profiles of Vanua Levu, 3-6, 62, 83, 107, 113, 153, 167, 173

Propylites, 68-72, 106, 147, 162, 181, 191, 199, 204, 214, 215, 268-270, 282, 297; origin of, 69, 72, 191

Pteropod-ooze deposits, description of, 320; mode of occurrence, 84, 86, 109, 139, 201, 205, 344

Pumice-tuffs, acid, 6, 207, 218-223, 229-233; general description, 336; special descriptions, 218, 220, 231

Pumice-tuffs, basic, 119, 333; _see_ Hyalomelan-tuffs

Pyroxene of groundmass, as a basis of classification, 236; _see_ Granular pyroxene, Prismatic pyroxene, Ophitic structure, and Synopsis

Pyroxene, rhombic, characters of, 285, 306; intergrowths with monoclinic, 266, 306

Pyroxene, derivation from hornblende, 306

Quartz, crystals of, 106, 191, 354; veins of, 106, 116

Quartz-andesites; _see_ Dacites

Quartz-porphyries, mode of occurrence, 215, 219, 220, 226, 227, 229-233; relative frequency, 235; general description, 309-311; distribution, 6, 207, 374

Quartz-rock, 139, 351, 354

Rainfall, 30, 68, 120

Rambi, island, 2; hot springs, 22

Ravi-koro mountain, 159

Ravi-ravi, 94

Ravuka, 120; hot spring, 31

Renard, Prof., 293, 306, 338, 344

Rewa District in Vanua Levu, 95, 96

Rewa River, Viti Levu, changes at mouth, 16

Rhyolites, 209; _see_ Quartz-porphyries

Rhyolite-glass, 220, 311

Rhyolitic-tuffs; _see_ Pumice-tuffs, acid

Ridge-mountains, their general appearance, 2, 6, 146, 153, 185, 210, 374; their structure and mode of origin, 75, 145, 156, 165, 166, 171, 172, 177-180, 182, 188, 202, 210-212, 216, 234; final conclusion, 375

Rivers; _see_ under Ndreketi, Lambasa Sarawanga, Wainikoro, &c.

Rivers, eroding power of, 62

Rocholl, Mr. H., 29

Rosenbusch, Prof., 306, 344

Ruku-ruku Bay, 53, 269

Salt Lake District, 2, 6, 9, 192-196

Sarawanga Plains, 15, 129-132, 351, 356

Sarawanga River, 15, 62, 129-131

Satulaki, 176, 268

Savarekareka Bay, 190, 326

Savulu, 118

Savu-riti Mountain, 210, 212

Savu-savu Hot Springs, 21, 25-30, 189

Savu-savu Peninsula, 189-192, 288

Sawa-ndrondro, 185

Scirpodendron costatum (Giant Sedge), 79, 83

Scoriaceous lava; _see_ Lava flows

Sealevu District, 146, 155, 156

Sealevu Divide, 136

Seatovo Range, 73-75

Seatura, mountain, 2, 3, 56, 253, 261, 374; general description of, 61-72; old town of, 67

Sections across Vanua Levu, 62, 107; _see_ also Profiles

Seemann, Dr., 55

Sella, on magnetic rocks, 362

Semi-opal, 351, 353

Sesaleka Mountain, 3, 12, 53

Siliceous concretions, 81, 83, 96, 132, 135, 351-355

Siliceous rock, blocks of, 126, 355

Siliceous sinter, 24, 25, 32, 33, 37, 42

Silicification, conditions of, 358

Silicified corals, 10, 13, 81, 132, 135, 138, 139, 207, 221, 226-228; theory of their origin, 228, 357; general account of, 350-360

Silicified fern rhizome, 360

Silicified nullipores, 353, 354

Singa-singa, 110

Singatoka River, Viti Levu, 7

Skinner, Mr. S., 367

Skye, Isle of, magnetic rocks, 362

Smallwood, Mr., 196

Smythe, Colonel, 22, 195

Soapstones; _see_ Foraminiferous deposits

Sokena Ridge, 167, 169, 172

Solevu Bay, 75-78, 253

Solfataric action on rocks, 52, 69, 72, 191

Soloa-levu Mountain, 103-105, 115, 296, 305, 312, 374

Solomon Islands, 1, 2, 294, 359

Songombiau, 220

Soni-soni Island, 93, 94

Soro-levu Mountain, 172-174

Spence, Mr. F., 193

Spheroidal weathering in basalts, 57, 129

Stromboli, 214, 315

Submarine basaltic flows and eruptions; _see_ Basaltic submarine flows

Submarine plateau or platform of Fiji, 15, 18, 19, 56, 62, 72, 107, 372; different explanations of, 373

Submarine tuffs, 326-336

Sueni District, 163

Suess, Prof., on thermal springs, 39; on changes in the sea-level, 20, 377

Suva soapstone, 322, 376

Synopsis of classification of volcanic rocks, 239-249

Tachylyte or basic glass, 312, 337, 341, 343; _see_ Basic glass, Pitchstone, Hyalomelan, &c.

Tahiti, 3, 72, 84, 363

Talasinga Districts, 55, 57, 64, 128, 132, 133, 224, 352, 383

Tambia, district, 137; hot springs, 32

Tambu-lotu District, 104, 105

Tathelevu, 198

Tavia, mountain, 121; ranges, 121-123

Tavua, 65

Tawaki District, 209, 229, 230

Tembe, 213, 214

Tembe-ni-ndio District, 130, 131, 319

Tenison-Woods, Rev., 376

Thambeyu, mountain, 5, 167, 289, 315, 326; description of, 176-179

Thawaro Peak, 230

Thermal springs; _see_ Hot springs

Thiele, Mr., 21

Thoka-singa Mountain, 103, 249, 302, 305

Thombo-thombo; _see_ Naithombothombo

Thomson, Mr. J. P., 31, 135, 210, 225

Thongea, hot springs, 22; basalt, 85

Thoroddsen, on Hekla, 375

Thuku, Mount, 6, 231, 308-310

Thulanga; _see_ Uthulanga

Thurston Range, 5, 167, 176; _see_ Thambeyu

Tonga Group, 1, 378, 379

Tongalevu District, 62, 64, 279

Towns, old sites of mountain, 53, 67, 101, 102, 108, 156, 170

Trachytes; _see_ Oligoclase-trachytes

Tuffs, chapter on, 317-336; foraminiferous, 326-333; altered, 184, 187, 190, 332; dacitic, 125, 126; _see_ Pumice tuffs, acid and basic; Hyalomelan tuffs; Palagonite tuffs; Crush tuffs; mode of occurrence, 48, 90, 109, 119, 130, 156, 160, 177, 190, 205, 209, 215

Tunuloa District, 205

Tutu Island, 221

Ulu-i-matua, 75, 76

Ulu-i-mbau, 138, 139

Ulu-i-ndali, 3, 83, 87-90, 253, 370

Ulu-i-sori, 136

Underwood, Lieut., 364

Undu, district and promontory, 6, 10, 36, 228-234, 311, 360

Upheaval; _see_ Emergence

Urata, 184, 298

Uthulanga Ridge, 211, 286 (also named Thulanga)

Vakalalatha Lake, 15, 225

Valanga Range, 181-185

Valavala Bay, 203

Valeni, 122

Va Lili, 5, 140-146

Valleys, origin of, 2, 146, 151, 219

Vandrani, district, 139, 159; hot springs, 32

Vanua Mbalavu, hot springs, 22

Variolite, 150, 283, 313

Vatui, 54, 369

Vatu Kaisia, 5, 113-116, 296, 301, 305, 374, 375

Vatu-karoa, 209, 282

Vatu-karokaro, 54

Vatu-kawa, river, 151; district, 160

Vatu-kerimasi, 101

Vatu-lele Bay, 184

Vatu-levoni, 139

Vatuloaloa Hot Springs, 31

Vatu Mata, 103

Vatu-ndamu, 91

Vatu-tangiri, 136, 144

Vatu Vanaya, 101

Vatu Vono Point, 88, 89

Vatu-vono District, 121, 122

Viene District, 198

Visongo District, 221

Viti Levu, 7, 18, 350, 364, 372

Vitina, 223

Volcanic agglomerates, general description of, 314-316; their thickness, 110, 156, 171, 178, 315; mode of occurrence, 5, 79, 91, 110, 112, 117, 141, 143, 144, 149, 155, 156, 161, 169-172, 176-179, 188, 193, 213, 214; lying above submarine deposits usually palagonitic and often foraminiferous, 110, 141, 143, 149, 168, 169-171, 176-179, 188, 213, 214; _see_ Pitchstone-agglomerates and Landslips

Volcanic bomb-formation, 46-48

Volcanic mud deposits; _see_ Foraminiferous deposits

Volcanic necks, 54, 58, 90, 93, 95, 112, 183, 192, 230, 234, 253, 277, 283, 286, 375

Volcanic rocks, classification of, 235; distribution of, 374

Vuinandi Bay, 208

Vuinandi Gap, 175

Vuinasanga, district, 145; hot springs, 31

Vui-na-savu, river and district, 222, 223, 225

Vula Votu Peak, 176

Vungalei Mountain, 212, 213, 315

Vuni-ika Bay, 218

Vunikondi, 232, 233, 282

Vunimbele, 139; hot springs, 33

Vunimbua, district and river, 182, 183

Vunimoli, hot springs and district, 33, 138, 139

Vunisawana, district, 194; hot springs, 34

Vuni-tangaloa, 194

Vunivuvundi District, 87

Waikatakata, Natewa Bay, hot spring and district, 34, 203, 275

Waikawa Mountains, 201, 319

Wailea, bay and district, 46, 50

Wailevu River, 15, 138

Wai Mbasanga, Viti Levu, hot springs, 21

Waimotu District, 208

Wai Ndina, Viti Levu, hot springs, 21

Wainikoro, district, 217, 224-228, 356; coast, 219, 308, 310; river, 225

Wai-ni-ngio River, 151, 160

Wainunu, hot springs, 22; rainfall 68; river and valley, 62, 82, 83

Wainunu, plateau or tableland, 3, 82-87, 373; _see_ figures on pages 83, 107

Waisali District, 146, 151

Waisali Saddle, 146-148

Waiwai, 143-145

Waterfalls, 79, 141, 163

Wawa Levu Mountain, 101, 302, 304

Weed, Mr., on the origin of siliceous sinter, 38

Wichmann, Dr. A., on a continental condition of the Fiji Islands, 376; on hyalomelan tuff, 334; on flints and silicified corals, 350, 352, 360; on Kandavu andesites, 293; on the absence of quartz-andesites in the South Seas, 294, 309; _see_ the preface

Wilkes, Commodore, 11, 15, 19, 25, 363, etc.

Wittstock, Mr., 36, 47, 53

Yanawai coast, 95-97, 122

Yanawai, river and valley, 113-116, 121

Yanganga Islands, 2

Yanutha Point, 123, 284

Yaroi, 189, 325

Yasawa Group, 294

Zeolites, formation of, in palagonite, 338

Zeolitic palagonite-tuffs, 334

Zirkel, on intergrowths of rhombic pyroxene, 306; on palagonite, 343; on magnetic rocks, 361

THE END

R. CLAY AND SONS, LTD., BREAD ST. HILL E.C., AND BUNGAY, SUFFOLK.

--------------------- Footnote 1:

In the case of the island of Faro in the Solomon Group, I have described a similar process of island-building. (_Geology of the Solomon Islands_, p. 37.)

Footnote 2:

In 1897 I spent several months in travelling over this island and ascended, sometimes more than once, the three great volcanic mountains. Perhaps at some future time I may renew my examination of this interesting region.

Footnote 3:

Strictly speaking Korolevu indicated in the profile would not be visible.

Footnote 4:

Mariko is the native name of the Drayton Peak of the chart. Mbatini is the correct name for the Koro Mbasanga of the chart, the true Koro Mbasanga lying three miles to the north. Thambeyu is a native name for the Mount Thurston Range.

Footnote 5:

There has been some confusion in the native names of the peaks in this part of the island, which I have not been able to remove.

Footnote 6:

_A Year in Fiji_, 1881, pp. 22, 167.

Footnote 7:

_Geology of the United States Exploring Expedition_, 1849.

Footnote 8:

This height has been supplied from memory, as I omitted to refer to the exact level of the erosion line in my notes.

Footnote 9:

They were described to me as dry for a fortnight at a time. I was prevented from making more than an occasional visit to them.

Footnote 10:

_Atlas of the United States Exploring Expedition_, vol. i., Philadelphia, 1850.

Footnote 11:

This, however, is not the case with the recent changes at the mouth of the Rewa River in Viti Levu, where the bare sandy point of Lauthala has extended itself seaward between 500 and 600 yards since 1840, whilst Port Nukulau has shoaled a fathom in the same period. But I can find no evidence of any marked advance in the mangrove margins either towards Nukulau or on the Kamba side, the only change recognisable being in the bare _sandy_ point of Lauthala, the rapid extension of which has been such as to attract the attention of residents, both whites and natives. Dana, who was in this locality in 1840, remarks in the _Geology of the U.S. Exploring Expedition_, that he had learned from a person who had resided there for forty years that during this period the deposits had lengthened the river half a mile. When I was on the Rewa in 1897 I heard that the natives in old time could see Suva Point from Rewa. This is probably a native legend connected with the modern extension of Lauthala Point. (The charts compared in making the above measurement of the recent advance of this point were the plan of the Rewa Roads by Wilkes, in 1840, and the Admiralty charts 1757 and 905, the former of which was based on Lieut. Dawson’s survey in 1875, the last being corrected to 1897.)

Footnote 12:

Between Mathuata Island and the coast a change is indicated from 9-10 fathoms to 8-9 fathoms, north of Motua Island 12-13 to 11-12, and between Nangano and Thakavi 16 to 14 fathoms.

Footnote 13:

By referring to the chart it will be seen that extensive mud-flats occur at the mouths of the Sarawanga and Ndreketi rivers, where the land-margin is slowly advancing.

Footnote 14:

_United States Exploring Expedition_, vol. x.; _Geology_, by J. D. Dana, p. 343.

Footnote 15:

_A Year in Fiji_, by John Horne, London, 1881, p. 163.

Footnote 16:

Journal, _Royal Geographical Society_, 1857, vol. 27.

Footnote 17:

_Scottish Geographical Magazine_, August, 1891.

Footnote 18:

_Journal des Museum Godeffroy_, heft 14, Hamburg, 1879.

Footnote 19:

Dr. Max Büchner also refers to this spring in his _Reise durch den Stillen Ozean_, 1878.

Footnote 20:

_Bulletin Museum Comparative Zoology_, Harvard, vol. 38; Geolog. Series V., No 1, Nov. 1900.

Footnote 21:

Amongst the other descriptions of these springs I may refer to that of Kleinschmidt in the work quoted on p. 22, to that of Miss Gordon Cumming in _At Home in Fiji_, to that of Horne in his _Year in Fiji_, &c. They are sketched in the descriptions of Kleinschmidt, Miss Cumming, and Commodore Wilkes. The analyses are given on a later page together with the references.

Footnote 22:

_Pacific Islands, Sailing Directions_, vol. ii., Central Groups, 1900, p. 185.

Footnote 23:

From what I remember the usual exposure at low-water in 1898 was less than a foot. I have little doubt as to the identity of the locality. This rock is one of the “sights” of the place at the present time. It would be interesting for a resident to compare carefully its present condition with that as described by Wilkes. Dana in the work quoted on p. 10, refers to this rock as a knoll of basalt; but he never visited the locality and only obtained his account from the officers of Wilkes.

Footnote 24:

_Narrative of the United States Exploring Expedition_, III., 199, by Commodore Wilkes. See also Dana’s _Geology_ of the same expedition.

Footnote 25:

_Journal des Museum Godeffroy_, heft 14, Hamburg, 1879.

Footnote 26:

_Islands of the Pacific_, by H. Stonehewer Cooper, 1888 edition.

Footnote 27:

_Journal Royal Society_, New South Wales, 1880, vol. 14. Miss Gordon Cumming in _At Home in Fiji_ gives the same analysis but differently stated.

Footnote 28:

To avoid error, I have given the results of each without converting them to a common standard. The numbers in brackets are taken from the form of Prof. Liversidge’s analysis given in Miss Gordon Cumming’s book.

Footnote 29:

_United States Exploring Expedition_, vol. 10, Geology.

Footnote 30:

_Proceedings_, Queensland Branch, Geographical Society, Australia, vol. 1. 1886.

Footnote 31:

I took the temperature at monthly intervals between October, 1896, and September, 1897. The mean annual temperature of the air in the shade would be about 64° at an elevation of between 3,000 and 4,000 feet.

Footnote 32:

At Ewa there are pumping plants capable of supplying 75 million gallons a day, the water being drawn entirely from artesian wells. (_Report on Hawaii_, by Dr. Stubbs, bulletin 95, 1901; U.S. Department of Agriculture.)

Footnote 33:

This hill is figured in Wilkes’ narrative under the name of Dillon’s Rock (vol. 3, p. 235). This, however, is not the Dillon’s Rock of his chart, where the name is given to a rock on the west side of the entrance to Wailea Bay.

Footnote 34:

See remarks on “crush-tuffs” on p. 334.

Footnote 35:

Species not identified.

Footnote 36:

In one of my traverses I crossed a level district extending a mile N.E. of Ndriti without changing my elevation.

Footnote 37:

At Delanasau, on the north or dry coast of the island, the average rainfall, according to many years’ observations by Mr. Holmes, is about 115 inches. At Wainunu, near the wet or south coast, the observations of Mr. Barratt and others extending over 16 years give an average of 160 inches. In the mountains this would be nearly doubled.

Footnote 38:

This question, which has so often been raised with respect to the propylites, will probably receive a different answer from different localities. The matter is further discussed on later pages.

Footnote 39:

The dyke-rock has a specific gravity of 2·7; but is slightly vesicular. It shows a few small plagioclase phenocrysts in a groundmass of felspar-lathes, augite grains and prisms, magnetite, and a little brown interstitial glass. The felspar-lathes average ·14 mm. in length and are for the most part not parallel. Secondary calcite occurs in the groundmass, and the powdered rock effervesces a little in an acid.

The rock forming the offshoot of the dyke differs only from the parent rock in its more vitreous character. Although the felspars and augites of the groundmass are fairly developed, the residual glass is much more copious, and in places where it has segregated, forming “lakelets,” it has been subjected to an alteration often observed in palagonite when there are concentric alternating zones of a tan-coloured fairly refractive material and calcite.

The reddish scoriaceous lava in contact with the dyke shows no phenocrysts. The groundmass displays more or less parallel felspar-lathes, ·1 mm. long, augite grains, and much magnetite. The residual glass is fair in quantity; but is mostly gathered into “lakelets” of brown altered glass with sometimes calcite in the centre.

The vitreous border of the dyke is composed of a dark glass quite opaque in the outer portion, but clearer and showing incipient crystallisation in the inner portion.

Footnote 40:

_Characteristics of Volcanoes_, 1890.

Footnote 41:

Referred to genus 16 of the olivine-basalts.

Footnote 42:

This subject is discussed in Chapter XXVI.

Footnote 43:

“Na Savu” is the Fijian for waterfall. The complete name of this fall is “Na Savu ni nuku.”

Footnote 44:

The flinty concretions are described on page 354, and the iron sand on p. 356.

Footnote 45:

_Geology of the United States Exploring Expedition._

Footnote 46:

A similar arrangement was observed in the columnar basalt of Kauai in the Hawaiian Islands. It is presumed that these Hawaiian flows are sub-aërial.

Footnote 47:

The unaltered glass, which incloses a few plagioclase phenocrysts, has a specific gravity of 2·7, and is readily fusible.

Footnote 48:

They are described on p. 322.

Footnote 49:

This absence of a healthy forest-growth, such as occurs on the level summit of the neighbouring Soloa Levu and in all like situations, has probably some geological significance.

Footnote 50:

These tuffs are probably submarine. They will be found described with tuffs of the same character on p. 333.

Footnote 51:

The track attains an elevation of about 1,300 feet, but the top of the watershed is two or three hundred feet lower.

Footnote 52:

It belongs to the 3rd order of the hornblende-hypersthene-andesites described on p. 299.

Footnote 53:

Occasional views of its summit only are obtained from the eastward, as from the Ndrandramea mountains and their vicinity.

Footnote 54:

Alluvial gold has long been known to occur in the bed of the Yanawai below Vatu Kaisia; but it has never been found in paying quantity.

Footnote 55:

Under the microscope it is shown to be granular in structure, exhibiting a mosaic of irregular quartz grains.

Footnote 56:

The blocks of the agglomerate in this last locality are from one to three feet across.

Footnote 57:

It displays in the groundmass augite prisms in flow-arrangement, and is referred to genus 20 of the augite-andesites.

Footnote 58:

Referred to genera 16 and 20 of the augite-andesites.

Footnote 59:

These foraminiferal limestones are described on p. 319.

Footnote 60:

_Proceedings_, Queensland Branch, Geographical Society of Australasia, Brisbane, 1886, vol. i.

Footnote 61:

_Geology of the United States Exploring Expedition._

Footnote 62:

_Pacific Islands_, vol. ii. 1900.

Footnote 63:

It is referred to the 5th sub-order (genus 18) of the hypersthene-augite-andesites characterised by prismatic pyroxene and more or less parallel felspar lathes in the groundmass, as described on p. 289. It displays abundant opaque porphyritic plagioclase giving extinctions of oligoclase-andesine. The pyroxene phenocrysts have dark alteration-borders. There is a little altered interstitial glass. Spec. grav. 2·55.

Footnote 64:

I did not ascend to the top of Ulu-i-mbau. It is, however, evidently composed of basic andesitic rocks, occasionally amygdaloidal. On its slopes up to at least 600 feet above the sea occur agglomerate-tuffs and finer submarine tuffs, as above described, overlying foraminiferous clays, a submergence of quite 500 feet being indicated by the investing deposits.

Footnote 65:

I did not find any foraminiferal shells or other organic remains either in this tuff or in the similar tuffs occurring on the adjacent slope of Va-lili up to 1,100 feet. My specimens, however, are very small.

Footnote 66:

It rises in the background of the view.

Footnote 67:

They are described under sample E on p. 332.

Footnote 68:

Referred to genus 37 of the olivine-basalts.

Footnote 69:

On the right side of the river close to Vatu-kawa there are some cliffs displaying a section of the mountainous spur, referred to on p. 151, that separates the valleys of the Mbale-mbale and Vatu-kawa rivers, an exposure quite apart from the rocks exhibited on the adjacent southern slopes of the main range. These cliffs are formed of bedded grey tuffs marked by single layers of blocks 6 to 8 inches across and dipping about 30° S.S.W. The tuffs in their texture are not unlike sub-aerial tuff-deposits. They contain no lime and are composed of basic materials with a little palagonite. They seem to indicate some subsidiary vent, close to the present village of Vatu-kawa, which may have been active shortly before or during the emergence of this district.

Footnote 70:

These altered tuffs on the southern slope of this range are described on p. 332.

Footnote 71:

Referred to genus 16, species A, sub-species 1, of the augite-andesites.

Footnote 72:

Referred to genus 9, sub-genus A, of the augite-andesites.

Footnote 73:

Referred to genus 9, sub-genus B, of the augite-andesites.

Footnote 74:

Both these rocks belong to the hypersthene-augite andesites, showing phenocrysts of both monoclinic and rhombic pyroxene. The first belongs to the orthophyric order described on p. 290; whilst the second belongs to the second order (genus 13, p. 287) where the felspars of the groundmass are lathe-like and in flow arrangement.

Footnote 75:

The highest dyke trends N. 48° E. and is inclined from the vertical about 15° N.W. The dyke, 5 or 6 yards below it, trends N. 30°E. and is vertical. The dyke, 50 yards farther down, trends N. 35° E. and is inclined from the vertical about 5° N.W. The inclination was only estimated. The bearings are true.

Footnote 76:

Both the types are referred to genus 1 of the augite-andesites, the olivine, when present, being quite insufficient to give a character to the rock. They however belong to different species according to the length of the felspar-lathes, which in the doleritic rocks averages ·2 mm. and in the other type ·08 mm.

Footnote 77:

It is pointed out on p. 5 that this name is wrongly applied in the Admiralty charts to Mount Mbatini, a mountain about three miles south of it.

Footnote 78:

Referred to genus 13 of the augite-andesites.

Footnote 79:

They are blackish and somewhat compact (sp. gr. 2·67-2·71) and have very small felspar-lathes less than ·1 mm. long. They contain both rhombic and monoclinic pyroxene, and are referred to genera 1 and 13 of the hypersthene-augite-andesites.

Footnote 80:

I discovered this error in a rather practical fashion by ascending the wrong mountain. The natives were engaged to take me to Koro-mbasanga and they performed their task, my aneroid and compass soon indicating that I was not on the highest peak of the island, but on a lesser peak three miles north of it.

Footnote 81:

Vula Votu is the name of a peak lying to the east. Ngoinangai is a forked mountain still further east.

Footnote 82:

A kind of “edible” bird’s-nest is found in this cave.

Footnote 83:

This rock is described on p. 251.

Footnote 84:

It is described under Sample C on p. 325.

Footnote 85:

It is granular, but fuses in the blowpipe flame into a clear glass and gelatinises in HCl. Probably a form of natrolite.

Footnote 86:

It is described under Sample D on p. 326.

Footnote 87:

_Ten Months in Fiji_, London, 1864.

Footnote 88:

_A Year in Fiji_, pp. 154, 169; London, 1881.

Footnote 89:

It displays an abundance of small phenocrysts of plagioclase, augite, and olivine partly serpentinised, in a groundmass composed in the main of coarse augite grains (·025 mm. in size) and of felspar microliths (·07 mm. in length) in smaller proportion, with little if any residual glass. Specific gravity 2·98. It is near the Waikawa basalt, referred to on p. 202, and is placed in the same genus (13) of the olivine class.

Footnote 90:

They are described on p. 269 under the non-porphyritic sub-genus of genus 2 of the augite-andesites.

Footnote 91:

These rocks are in most cases referred to the orthophyric and felsitic orders of the hypersthene-augite andesites. The rocks of the last-named order prevail, and form the type of the group, as described on p. 291.

Footnote 92:

It belongs to genus 37 of the olivine class. The felspar-lathes average 0·2 mm. in length, and there is a little altered interstitial glass.

Footnote 93:

It is referred to genus 16, species D, of the augite-andesites. The felspar-lathes have an average length of ·3 mm.

Footnote 94:

_Proceedings_, Queensland Branch, Geographical Society of Australia, vol. i.; 1886.

Footnote 95:

Referred to genus 9 of the augite-andesites.

Footnote 96:

The general characters of these rocks are described on p. 308.

Footnote 97:

_Geology of the United States Exploring Expedition._

Footnote 98:

_A Year in Fiji_, p. 22.

Footnote 99:

Described on p. 310.

Footnote 100:

These rocks are described on p. 308.

Footnote 101:

It contains small phenocrysts of plagioclase (medium andesine), and of augite and rhombic pyroxene, and is referred to genus 1 of the hypersthene-augite andesites.

Footnote 102:

See paper quoted on p. 31. It is noteworthy that Mr. Horne refers only to a single floating island.

Footnote 103:

_Journal_, Royal Geographical Society, June, 1894.

Footnote 104:

Described on p. 309.

Footnote 105:

Described on p. 310.

Footnote 106:

Referred to genus 13 of the augite-andesites. The felspar-lathes average ·1 mm. in length, and there is a little interstitial glass.

Footnote 107:

Referred to genus 16 of the augite-andesites. There are two sets of felspar-lathes in the groundmass; the larger, ·23 mm. long, are more or less parallel; the smaller, ·04 mm. long, form a plexus.

Footnote 108:

Each division would theoretically also possess an orthophyric and a felsitic order; but these orders are not represented in my collection and need only be mentioned.

Footnote 109:

Not represented in the collection.

Footnote 110:

I apply the term “diorite” to granitoid rocks formed entirely of plagioclase and hornblende.

Footnote 111:

According to the size of the plagioclase phenocrysts, whether averaging less than or more than 3 mm. in size, these rocks may be divided into a non-porphyritic and a porphyritic sub-genus.

Footnote 112:

_Petrographie des Viti Archipels_; Miner. und Petrogr. Mittheil; band v, heft 1, Wien, 1882.

Footnote 113:

_Physics and Chemistry_, II. Report Scient. Results; H.M.S. Challenger; London, 1889.

Footnote 114:

_Petrographical Notes on the Fiji Islands_; Proceed. Amer. Acad. Arts and Sciences; vol. 34; no. 21; May, 1899.

Footnote 115:

_Notes on the Limestones and General Geology of the Fiji Islands_, Bull. Mus. Comp. Zool, vol. 5. Geolog. Ser. vol. 5, no. 1, Cambridge, Mass., U.S.A. Nov. 1900.

Footnote 116:

Wichmann describes rocks from the cliffs of the Singatoka river and from Ovalau.

Footnote 117:

_Geology of the Solomon Islands_, by H. B. Guppy, 1887, pp. 6, 36.

Footnote 118:

The term “felsitic andesite” is suitable for this microfelsitic type.

Footnote 119:

I have borrowed this term from Rosenbusch’s _Microscopical Physiography of the Rock-making Minerals_, translated by Iddings.

Footnote 120:

_Challenger Reports_, Physics and Chemistry II.

Footnote 121:

_Neues Jahrb. fur Mineralogie_, 1884.

Footnote 122:

For their mode of occurrence, see pp. 215, 220, 230-233.

Footnote 123:

Highly altered rocks of this class are exposed at the base of Mount Nailotha as described on p. 215.

Footnote 124:

See work quoted on p. 218.

Footnote 125:

See p. 230.

Footnote 126:

_Quart. Journ. Geolog. Soc._ xliv. 1888.

Footnote 127:

Zirkel’s _Petrographie_, iii., 694.

Footnote 128:

This basalt is not fusible in the ordinary blow-pipe flame.

Footnote 129:

In this connection see the description of the Soloa-levu pitchstone on p. 312.

Footnote 130:

See the note at the end of this chapter.

Footnote 131:

Quoted in Zirkel’s _Petrographie_, iii., 689.

Footnote 132:

I have visited this locality on several occasions with the special object of studying the relation of the basalt to the associated palagonite-tuffs and clays. A general discussion of this question would be out of place here; but I may remark that the conclusion arrived at by me is that these deposits are not sedimentary but are entirely the result of the disintegration of palagonite _in situ_. This is quite opposed to the view of their sedimentary origin held by Dr. Johnston-Lavis, Prof. Platania, and other Italian geologists.... The basalt is scoriaceous, semi-vitreous, and semi-ophitic, and closely approaches the type of basalt above defined.

Footnote 133:

_Reisen auf den Viti-Inseln_, as quoted on p. 22.

Footnote 134:

_Petrographie des Viti-Archipels_, quoted on p. 293.

Footnote 135:

See work quoted on p. 378.

Footnote 136:

_Solomon Islands and their Natives_, by H. B. Guppy, p. 78.

Footnote 137:

The region is described on pp. 224-228.

Footnote 138:

For the meaning of “talasinga” see p. 55.

Footnote 139:

The portion exhibiting the coral structure has a specific gravity of 2·54.

Footnote 140:

A good list of references to the early German authorities on the subject is given in the _American Journal of Science and Arts_ for 1831, vol. 20.... Zirkel in his _Lehrbuch der Petrographie_ (1893, vol. i. p. 565) gives most of these and many more recent.... Harker in his paper below named refers to a review of the earlier literature in _Verh. naturh. Vereins_. Bonn, 1851, vol. 8, and to a more complete bibliography by Meli in _Boll. Soc. Geol. Ital._ 1881, vol. 9.... British Association Report in 1889 by Professors Rücker and Thorpe on the Magnetic State of the British Isles.... _Nature_ for August and September, 1894, &c.... Harker on magnetic disturbances in the Isle of Skye, _Proc. Cambr. Philos. Soc._ vol. 10, part 5.... Skinner in _Proc. Cambr. Philos. Soc._ May, 1894.... Clark in _Journ. Roy. Instit._ Cornwall, 1890-93.... Folgheraiter in _Frammenti concernanti la geofisica_, Rome: referred to in _Nature_, July 27, 1899, and Nov. 8, 1900.

Footnote 141:

Nearly all volcanic rocks at all basic are magnetic, owing to the constant presence of magnetite; but magnetic polarity, when the rock-fragment has a negative and a positive pole, is not directly concerned in volcanic rocks with the mineral composition.

Footnote 142:

Some of the earliest observations were made on granites and trachytes.

Footnote 143:

_Geology of the United States Exploring Expedition_, 1849, p. 294.

Footnote 144:

_Quarterly journal Geological Society_, vol. li., p. 469.

Footnote 145:

Wilkes’ _Narrative of the U.S. Exploring Expedition_, iii., 185.

Footnote 146:

Of the tuffs and clays, almost all submarine and often containing tests of foraminifera and sometimes molluscan shells, about 90 per cent. exhibit simple magnetism in a slight degree, but out of nearly 100 specimens tested none show polarity.

Footnote 147:

On p. 357 will be found some notes on the magnetic iron sand that occurs in great abundance in river and stream beds.

Footnote 148:

These values represent the number of degrees that the magnetic needle is repelled. The method is described above. A note on the average amount of polarity found in all my polaric rocks is given at the end of the chapter. The term “dacite” _is here an equivalent_ of “felsitic andesite.”

Footnote 149:

This name has been wrongly applied in the Admiralty chart to the mountain of Mbatini. Koro-mbasanga, 2,500 feet, lies three miles to the north.

Footnote 150:

This rock is described on p. 109. There is no exceptional development of magnetite for a basic rock in the groundmass.

Footnote 151:

Unfortunately, I have no data for the peaks of Na Raro and Vatu Kaisia, except that specimens obtained below the summits are non-polaric. In the case of Na Raro I did not retain the specimen obtained at the top; whilst in my ascent of Vatu Kaisia I did not quite reach the summit.

Footnote 152:

The mode of measurement is described on p. 366.

Footnote 153:

See pp. 2, 15, 18, 56, 62, 72, &c.

Footnote 154:

_The Islands and Coral Reefs of Fiji_, Bull. Mus. Comp. Zool. Harv. Coll. vol. 33, 1899.

Footnote 155:

_Scott. Geogr. Mag._ 1895.

Footnote 156:

_Ancient Volcanoes of Great Britain_, by Sir A. Geikie, 1897, ii. 260.

Footnote 157:

See Wichmann in _Min. und Petrog. Mitth._ band v. heft 1.

Footnote 158:

_Amer. Journ. Sci._ VI. 165, 1898. See also Agassiz on the _Islands and Coral Reefs of Fiji_, before quoted.

Footnote 159:

_Proc. Linn. Soc._ N.S.W. 1879-80, p. 358.

Footnote 160:

_Quart. Journ. Geolog. Soc._ vol. 44, 1888.

Footnote 161:

See Preface to the report of Mr. Andrews quoted on a later page.

Footnote 162:

_Das Antlitz der Erde_, French edition by E. de Margerie, ii. 534.

Footnote 163:

See the paper before quoted on the coral reefs of Fiji.

Footnote 164:

_Bull. Mus. Comp. Zool._ Harv. Coll. vol. 38. _Geolog. Ser._ vol. 5, no. 1, 1900. _On the Limestones and General Geology of the Fiji Islands_, by E. C. Andrews.

Footnote 165:

_Quart. Journ. Geolog. Soc._ vol. 47, p. 590, 1891. See also Mr. Harker’s paper below quoted.

Footnote 166:

_Geolog. Mag._ June, 1891.

Footnote 167:

Seemann’s _Flora Vitiensis_, Horne’s _Year in Fiji_, Hillebrand’s _Flora of the Hawaiian Islands_, Hemsley’s “Flora of the Tonga Islands” in _Journal Linnean Society_, Botany, vol. 30.

Footnote 168:

See Hutton _Proc. Linn. Soc._ N.S.W. 1896, Baur, _Amer. Nat._ 1897, Pilsbry, _Proc. Nat. Sci. Philad._ 1900, Hedley, _Proc. Linn. Soc._ N.S.W. 1892, 1899, &c.

Footnote 169:

The term “basalt” is here used in a general sense to include olivine-basalts, basaltic andesites, and other basic types of the augite-andesites and hypersthene-augite andesites.

Footnote 170:

The usual signification of “koro” as a prefix or part of names of hills and mountains is a “prominence” or “projection.” It is a mistake on my part to assume that in such cases it is as a rule equivalent to a town or village.

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Transcriber's Note

There is some inconsistent spelling and hyphenation in this book which has not been normalized.

Some corrections have been made to the text. In particular, punctuation was corrected. Additionally, the following changes have been made:

p. 10 beween -> between p. 75 ·15 m. long -> ·15 mm. long p. 114 ts -> its p. 208 aud -> and p. 244 Pyroxyene -> Pyroxene p. 270 adoped -> adopted p. 345 tea-estat -> tea-estate