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 INGINEERING LIBRARY 
 
Cornell University Library 
 QE 264.G78K5 1877 
 
 Explanation of sheet 9.Kirl(cudbright no 
 
 3 1924 004 137 182 
 
Cornell University 
 Library 
 
 The original of tiiis book is in 
 tine Cornell University Library. 
 
 There are no known copyright restrictions in 
 the United States on the use of the text. 
 
 http://www.archive.org/details/cu31924004137182 
 
«p 
 
 SCOTLAND. 
 
 EXPLANATION OF SHEET 
 
 9. 
 
 KIRKCUDBRIGHT (NORTH-EAST PART) AND DUMFRIES- 
 SHIRE (SOUTH-WEST PART). 
 
 EDINBURGH: 
 
 ^•V PRIUTBD FOR HER MAJESTY'S STATIONkfiT OFFICE, 
 
 "'- AND SOLD _BT ,. , 
 
 W. & A. K. JOHNSTON, 4 ST. ANDREW SQTTARE ; 
 
 ALSO IN LONDON BT 
 
 Stantoed, 6 Chaeing Cross, W.C. ; Letts & Son, Rotal IJxohan&e, E.G. ; 
 liONGMAN & Co., Pateenostbr Row ; AND Wyld, 11 AND 12 Charing Cross ; 
 
 AND IN DUBLIN BT 
 
 Hodges, Foster, & Co., 104 Grafton Street. 
 18 7 7. 
 
 Price One Shilling^. 
 
ISTB JiX 
 
 to tlLe 
 
 GEOLOGICAL SURVEY MAP 
 
 of 
 
 PuiTisJud'on^Scale'OfOne'inchtoa^mile 
 June, 1877. 
 
 \ Published' 
 
 A In pi'eparatLmv 
 
 KJ Memoirs pitiUsJud L 
 
SCOTLAND. 
 
 EXPLANATION OF SHEET 
 
 9. 
 
 KIRKCUDBRIGHT (NORTH-EAST PART) AND DUMFRIES- 
 SHIRE (SOUTH-WEST PART). 
 
 EDINBURGH: 
 
 PRINTED FOR HER MAJESTY'S STATIONERY OFFICE, 
 
 AND SOLD BT 
 
 W. & A. K. JOHNSTON, 4 ST. ANDREW SQUARE ; 
 
 ALSO IN LONDON BY 
 
 Stanford, 6 Chaking Cross, W.C. ; Letts & Son, Rotal Exchange, E.G. ; 
 Ijongman & Co., Paternoster Row; and Wtxd, U and 12 Charing Cross; 
 
 AND IN DUBLIN BT 
 
 Hodges, Foster, & Co., 104 Grafton Street. 
 18 7 7. 
 
PEEFACE. 
 
 The axea embraced in Sheet 9 of the Geological Survey of Scotland 
 was surveyed by Mr. H. M. Skae, Mr. John Home, Mr. C. Campbell, 
 and myself Mr. Skae mapped the ground to the east of the Nith, 
 except the Permian rocks of the Thornhill and Dumfries basins. Mr. 
 Home's tract embraced the country lying westwards from the Nith 
 Valley, except the central tract enclosed within a line drawn from 
 Moniaive, south-westwards by Loch Skae to New Galloway, and down 
 the Ken Valley to Parton ; thence eastwards by Kirkpatrick-Durham, 
 to the line of railway, and northwards by Loch Eutton and Dunscore 
 to Moniaive. In the area thus enclosed, the Silurian rocks were first 
 mapped by Mr. Campbell, whose work was subsequently revised and 
 connected with that in the surrounding districts by Mr. Home ; while 
 the Survey of the drift deposits, in the same area, was shared by 
 Mr. Home and Mr. Irvine. The Carboniferous and Permian rocks of 
 the Thornhill basin were mapped by myself, in conjunction with 
 Messrs. Skae, Home, and Campbell. 
 
 To the following Explanation, Mr. Home contributes paragraphs 
 1-12, 1V16, 18-27, 30-32, 33-36, 72-78, 80-88, 90-101 ; Mr. Skae, 
 Nos. 13, 17, 33, 58, 68, tl, 79, and 89 ; Mr. R. Etheridge, jun., Nos. 
 28 and 29 ; while I have suppHed Nos. 37-70 (except Nos. 58 and 68). 
 The Fossil Lists in the Appendix are by Mr. R. Etheridge, jun. The 
 list of papers referring to the geology of the district has been drawn 
 up by Mr. Home. 
 
 AECH. GEIKIE. 
 
 Geological Survey Office, 
 Edinburgh, June 1877. 
 
EXPLANATION OF SHEET 9. 
 
 I. AEEA EMBRACED IN THE MAP. 
 
 1. This sheet embraces 432 square miles of ground, stretching from 
 Cairnsmore of Carsphairn, eastwards by Shinnelhead, Carronbridge, 
 to the sources of the Capel Water, southwards by Dairy and New 
 Galloway to the foot of Loch Ken, then eastwards by Kirkpatrick- 
 Durham and the Mabie HiUs to Kirkconnell Moss. It includes that 
 portion of the Vale of the Nith which extends from Drumlanrig to 
 Dumfries, along with the valleys of the Cairn and the Ken, and the 
 northern portion of the Urr. The county boundary, which crosses the 
 Map, divides it into nearly equal parts. All the ground to the east 
 and north of this line lies in Dumfriesshire, while the remainder 
 belongs to the county of Kirkcudbright. With the exception of the 
 southern half of the ThornhiU Permian basin and the northern portion 
 of the Dumfries basin, this area forms part of the Silurian belt which 
 stretches from sea to sea. 
 
 II. FORM OF THE GROUND. 
 
 2. The physical features of this area may be grouped in two divisions : 
 1st., the rich low-lying ground enclosed within the Thornhill and Dum- 
 fries basins ; 2d., the scenerjf" which is peculiar to the Silurian and 
 Granitic regions, which occupy the rest of the Map. 
 
 3. The basins already mentioned contain the main stretches of low 
 ground met with in this sheet. They are encircled by ranges of hills 
 of no great elevation. The Dumfries basin, for example, is hemmed in 
 on the west by the Mabie, Terregles, and Dunscore Hills, which vary 
 in height from 600 to 800 feet ; while the Kirkmahoe and Tinwald 
 HUls bound it on the north and east respectively. And so the low 
 ground in the neighbourhood of Thornhill is flanked by the Keir Hills 
 on the west, and by the steep heathery slopes of the Closeburn Hills 
 on the east. A glance at the Map will show that these marked features 
 coincide roughly with geological boundaries. Within these limits the 
 ground is richly cultivated, but beyond them the scenery is mostly of 
 a different type. It is important to note that these basins are not 
 continuous. They converge abruptly, and a narrow valley about three 
 and a half miles in length, along which the Nith flows, connects the two. 
 
 4. Although the wide Silurian tract presented in this Map forms part 
 of the great Silurian table-land of the southern uplands, yet it cannot 
 be said to include a range of hills of any importance. The ground 
 is everywhere hilly, rising in places to considerable elevations; but 
 nowhere in the sheet is there any prominent mass of high ground 
 
west of Loch Ken, and the remaining portion being confined to a 
 narrow strip extending from Whinnyhill to Lochaber Loch. Each of 
 these granitic areas is surrounded by a ring of metamorphosed strata 
 of varying breadth. 
 
 Lower Silurian. 
 
 7. Those subdivisions of the Llandeilo rocks, which, with certain 
 modifications, have been found to extend along the Silurian range of 
 the south of Scotland, are traceable across this sheet. The general 
 succession of the various groups, which has been established in areas 
 already described by the Geological Survey, in the Lead Hills and 
 Wigtonshire, is borne out by the evidence obtained in this district. 
 A line drawn from Dundeugh Hill at the junction of the Deugh with 
 the Ken, north-eastwards by Stroanfreggan, Carlae Hill, Mullwhanny, 
 and Shinnelhead, coincides with the axis of a synclinal trough. North 
 of this line the general dip of the beds is towards the south-east, while 
 on the south side the prevailing dip is to the north-west. This well- 
 marked trough can be traced still farther to the north-east in Sheet 15, 
 by Chanlockhead, Hallscar Craig, rardingmuUach Moor, Eliock Wood, 
 to the north edge of the Carron Permian basin. The syncline here 
 described as extending over an area of twenty miles, does not seem to 
 be continuous with the great trough of the. Lowther range, as will be 
 explained in a subsequent paragraph, but appears rather to ' nose out ' 
 near the limits of the Permian basin. The centre of this trough is 
 occupied by the uppermost members of the Llandeilo series, while 
 strata belonging to a lower horizon dip underneath on both sides. 
 
 8. A section drawn from the centre of this trough along the course 
 of the Dalwhat Water, by Moniaive and Glenessland to the Mabie 
 granite, would show the innumerable foldings of these Silurian rocks. 
 Though the strata along this line describe a series of curves, yet on the 
 whole they form a descending series, so that the lowest beds are to be 
 found dipping away from the Mabie granite. The general strike is 
 from south-west to north-east, while the dip varies from 50° to 80°. The 
 effect of these rapid foldings has been to bring the same beds repeatedly 
 to the surface, so that the relative areas occupied by the respective 
 members of the series are no indication of the actual thickness of 
 strata. Even where beds of the same lithological character are found 
 to dip for some distance in one direction, it is highly probable that in 
 many cases they are repeated by inverted folds, though the truncation 
 of the arches by denudation has removed the proof. This fact, how- 
 ever, is capable of demonstration in those areas where different 
 members of the series, possessing distinct lithological characters, are 
 folded back on each other (pars. 10 and 12). From the fossil evidence 
 obtained, it has been inferred that representatives of both the Caradoc 
 and Llandeilo formations occur in the Map. The following classifica- 
 tion will shoT^ at a glance the nature of the various groups. These are 
 given in the order of succession, along with their respective thicknesses. 
 It will be seen that most of the groups described in Explanation to 
 Sheet 15, and all those which occur in Sheet 3, are likewise to be found 
 in this area, with one addition, which has been named the Carsphaim 
 Group. 
 
 o Feet. 
 
 2 ni ( Coarse conglomerates, with pebbles of quartz, quartz rock, greywaoke, 
 
 3 § ■! lydian-stone, and pieces of grey and black sliales containing 
 
 -4 M ( graptolites. Estimated thickness ...... 2000 
 
/(7.) Carsphaim Group.— Coavae pebbly grits, shading into fine con- 
 glomerates, along with greywackes and shaly partings lying 
 conformably in Group (6). Estimated thickness . . . 1200 
 (6.) Upper or Lead Hills Black Shale Group.— Black shales containing 
 graptolites, with bands of chert and thin-bedded grey shales. 
 
 Estimated thickness 65" 
 
 (5.) Lowther Group.— The characteristic feature of this Grou^ is a thick 
 series of soft grey shales, and hard blue shales, with hnely lami- 
 nated ilags and lenticular patches of grit passing occasionally 
 into pebbly bands, like the underlying ' Haggis rock. ' Estimated 
 
 thickness • ^250 
 
 (4.) Dalveen Group. — Thick and thin much-jointed greywackes, with 
 grey and blue shales, including a well-marked bed of fine con- 
 glomerate or pebbly gi-it called the 'Haggis rock.' Estimated 
 
 g / thickness .-.•." • . • ®'''"' 
 
 w \ (3-) Queensberry Group. — A great series of massive grits, with occasional 
 bands of conglomerate. The grits have a regular system of joint- 
 ing. Near the top there is a mass of shales several hundred feet 
 thick interbedded with the grits, known as the 'Barlae shales.' 
 At the base, and resting on the underlying group, there is a 
 considerable thickness of grey and blue shales, with occasional 
 flaggy greywackes, and grits occupying the position of the 
 
 'Grieston series.' Estimated thickness 4500 
 
 (2.) Lower or Moffat Black Shale Group. — Black shales containing 
 
 graptolites, with grey shales and yellow shattery clayey bands. 
 
 Estimated thickness . . . ■ . . . . 200 to 400 
 
 (1.). Ardwell Group. — Well-bedded brown flags and argillaceous shales, 
 
 and shattery brown and yellow-crusted sandy greywackes, with 
 
 \grey and purplish sandy shales, and occasional masses of red 
 shales. Thickness not ascertainable in this area. 
 
 Llandeilo Beds. 
 
 Ardwell Group. 
 
 9. This series of beds rises out from underneatli the outcrop of black 
 shales in the Glen Burn, in the parish of Kirkpatrick-Irongray. It 
 occupies the belt of country nearly six miles in breadth, lying between 
 this crop and the Mabie granite. The beds strike in a north-easterly 
 direction, and are overlaid unconformably by the Permian sandstones 
 of Dumfries. They are well exposed in the hills to the north of the 
 Mabie granite, in the railway cuttings between Goldielea and Lochan- 
 head, the Terregles Hills, and the streams draining to the east. 
 Perhaps the best section, which shows the relation of these beds to the 
 • overlying group, is to be found in the Old Water and its tributary the 
 Scar Burn. From Shawhead northwards to the outcrop of black shales, 
 the section is almost continuous. While several south-easterly dips are 
 to be met with in this section, the strata are, on the whole, inclined to 
 the north-west at an angle varying from 50° to 70°. This group consists 
 of yellow or ochreous crusted greywackes, sometimes sandy and mica- 
 ceous, with grey and purplish sandy shale, also hard flaggy bands with 
 pale argillaceous shales and occasional masses of red shales. Though, 
 the beds usually weather with a yellow or brown crust for about half 
 an inch, they are light-blue and grey in colour where a fresh fracture 
 can be obtained. The greywackes when exposed to weathering often 
 break under the hammer into small angular pieces ; but there are harder 
 fine-grained bands, which when quarried make admirable building 
 stones. These split up for the most part along certain joints which 
 are coated with pink and white calc-spar. Many of the greywacke 
 bands are seamed on the surface with veinings of quartz and carbonate 
 of lime. Cleavage is also of common occurrence among the masses of 
 
10 
 
 shales, but of so imperfect a nature that the beds rarely split along the 
 cleavage planes. 
 
 It is worthy of note that the beds which immediately underlie the 
 Lower or Moffat Black Shales in this district have a more shaly 
 character than in the Ardwell area in Wigtonshire. They form a well- 
 marked ribboned series which is seen to advantage in the Old Water. 
 One peculiar feature of this group is the constant change of dip over 
 the whole area, due to an incessant repetition of sharp plications. On 
 the coast line south of Gatehouse, in Sheet 4, these rapid undulations of 
 the strata are admirably exposed, there being sometimes about fifty 
 anticlinal and synclinal folds in the course of a mile. Owing to this 
 absence of any persistent dip, as well as to the metamorphism of the 
 strata round the granite, it is impossible to compute with any degree 
 of accuracy the thickness of the group in this district. The grey and 
 purplish shales have yielded specimens oi Protovirgularia, while traces of 
 graptolites have been met with at rare intervals. Many of the flaggy 
 bands are well ripple-marked. 
 
 10. In the metamorphic area to the west of New Galloway, there is 
 a narrow strip of brown crusted flags and shales about half a mile 
 broad, extending from Waukmill in the Knocknairling Burn to the 
 Lodge Knowes. This strip occurs between two parallel outcrops of 
 highly altered black shale. The latter, as well as the beds which 
 come between, dip to the north-west. But, from certain points of 
 resemblance between the strata at Shawhead and those north of Wauk- 
 mill, it is highly probable that there is here an inversion of strata ; the 
 altered black shales being brought up along an inverted arch which is 
 deep enough to expose a small portion of the underlying group. This 
 is rendered all the more probable from the fact that along the same 
 line of strike to the south-west, between Clatteringshaws and Newton- 
 Stewart, there is a reversed anticline of Ardwell beds, lying between 
 two similar outcrops of black shales which are not so highly metamor- 
 phosed. This fold can be traced, as will be pointed out in the Explan- 
 ation to Sheet 8, till it abuts against the granite near the Bridge of Dee 
 at Clatteringshaws. It is extremely probable, therefore, that this strip 
 of brown crusted beds, which reappears between Waukmill and the 
 Lodge Knowes, represents the eastern prolongation of this arch. These 
 beds are altered into grey spotted schists, which pass into regular mica 
 schists. They strike from 20° to 25° to the north of east, and seem to 
 ' nose out ' near Millbank above New Galloway. 
 
 Lower or Moffat Black Shale Group. 
 
 11. Though the beds included in this group are of no great thickness, 
 they form a definite horizon, in virtue of their marked lithological 
 character. The group consists of black and grey shales, with pale 
 yellow or whitish clayey bands. The prominent feature of the group 
 is the occurrence of persistent bands of black shales, which as a rule are 
 abundantly charged with graptolites and sometimes contain the small 
 brachiopod, Siphonotreta micula. They are interbedded, however, with 
 grey sandy shales which occasionally contain graptolites ; while pale- 
 coloured shattery bands of clay are usually associated with them. 
 The black shales as well as the clays are much broken by joints, and 
 the former are traversed by innumerable veinings of quartz. Owing 
 to their soft and yielding nature, the dark shales are much crumpled, 
 which renders the determination of their thickness a matter of some 
 difiBculty. As a result of the intense contortion which the strata have 
 
11 
 
 undergone, the members of this group often occupy a greater breadth 
 than their thickness would lead us to expect (par. 12). The rapid 
 puckerings of the shaly series is admirably seen in many of the 
 sections. The actual thickness of the group does not probably exceed 
 400 feet, while in some sections it may not be much more than 200 
 feet. 
 
 The main or south-east crop of the black shales is not traceable con- 
 tinuously across this sheet. In the valley of the Cluden it is buried 
 underneath a thick covering of drift, which sweeps round the south 
 face of Steilton Hill, and westwards along the south slope of the 
 Forrest Hill. It occurs, however, in the Scar Burn, the Old Water, 
 and along the course of the Glen Burn to the north slope of the Lar- 
 ganlee Hill, where it crops out close to the roadside, and is traceable, 
 by means of fragments on the surface, to the Brooklands Burn. A 
 wide stretch of boulder clay conceals the outcrop again for some 
 distance, but it reappears close to Barmofitty, and is traceable across 
 the sheet to the south. This crop is in the same line of strike as the 
 black shale bands which occur in the Glenkiln Burn to the north of 
 Kirkmichael Manse, first described by Professor Harkness. Although 
 the black shales form a definite horizon, it does not follow that they 
 are a continuous deposit ; it is highly probable if the drift were peeled 
 off the surface of the country, they might be found thinning out along 
 the normal line of strike. At any rate they mark oif the more thin- 
 bedded and shaly strata on which they rest from the overlying massive 
 arenaceous series. It is important to bear the latter fact in mind when 
 trying to unravel the structure of the ground to the north. 
 
 12. Owing to the plications of the overlying Queensberry group, the 
 Lower Black Shales reappear along certain anticlinal folds to the north 
 of the normal line of strike. The folds are rarely broad enough to 
 reveal the top of the Ardwell beds, as is the case to the west of New 
 Galloway. In some cases only a portion of the Lower Black Shale 
 group is brought to the surface, while the outcrops are not traceable 
 for any great distance. But this is what inight naturally be expected 
 in such a highly contorted area, for it is evident that though the black 
 shales may crop out repeatedly along certain axial folds, these anti- 
 clines may 'nose out ' to the north-east and south-west, so that the shales 
 pass underneath the beds lying at the base of the overlying group. 
 This is what actually does occur in many instances. The anticlines are 
 not always flanked by strata dipping in opposite directions, for in many 
 cases the beds have been inverted so that they appear to dip con- 
 tinuously in the same direction. A glance at the Map will show that 
 after several undulations, the members of the overlying group begin 
 to dip to the south-east in the Drumhumphry and Auchenhay Burns to 
 the east of Corsock. The black shales soon reappear in the latter 
 section, and a little way to the north-west in the Water of Urr 
 numerous outcrops are to be met with. Along the same line of strike 
 to the north-east they occur in the Glenessland Burn and its tributaries, 
 while to the south-west they are to be found in the Crogo, Auchenvey 
 and Barend Burns. About two miles to the north-west of the general 
 strike of these outcrops, the black shales are brought up by another 
 anticlinal fold, about a mile to the west of the Lowes Lochs. In the 
 metamorphic area to the west of Loch Ken, on the Bennan Hill, there 
 are some bands of highly altered dark shales, which seem to be meta- 
 morphosed representatives of this group. These will be referred to 
 along with the other metamorphic rocks. They strike in a northerly 
 direction towards the Shirmers, and are inclined to the N.N. W. at a high 
 
12 
 
 angle. To the west of New Galloway there are two parallel outcrops 
 of similarly altered dark shales, which are confined to the metamorphic 
 area ; the one may be seen near the roadside at Lodge Knowes, and the 
 other, which occux-s about half a mile to the south, is traceable from 
 Waukmill to the edge of the granite. These dark bands are hardly 
 recognisable as black shales close to the granite. Both crops dip 
 north-north-west at an angle of from 50° to 60°., but from the nature of 
 the beds between, as well as from the character of the shaly series to 
 the north and south of the black shales, it is inferred, in spite of the 
 apparent dips, that the strata are folded back on each other. No fossils 
 have been found within the metamorphic zone. Again, about two miles 
 to the north of Dairy, the black shales reappear in the Ken and in the 
 burn north of Barskeoch Mains. In this case also, the dark shales, as 
 well as the strata on both sides, are inclined to the north-west. The 
 latter consist of coarse grey grits with dark-blue shaly bands, and are 
 evidently repetitions of the same beds. 
 
 It is worthy of note that the most frequent outcrops of black shales 
 occur in the south-western part of the sheet. From Auldgirth north- 
 westwards by the Keir Hills to the limit of the Queensberry series, no 
 representatives of this well-marked group have been found, although 
 the rocks are well exposed in the streams and hill slopes. The gritty 
 series is probably as much folded in the one case as in the other, 
 though the anticUnes are not sharp enough to expose the underlying 
 beds. 
 
 13. These shales, as already mentioned, are exposed east of the Nith 
 in the Glenkihi Burn, a little way above the Manse of Kirkmichael. 
 From thence a prolongation of the strike carries the line of probable 
 outcrop south-west by Whitstanes to Dalswinton. Brought up by a 
 sharp anticlinal fold, the black shales are again seen in the Gapel Burn 
 about a mile to the south of Mitchellslacks, and close to its junction 
 with the Poldivar Lake Burn. To the east of this they can be traced 
 from the Bran Burn running up the shoulder of Wee Queensberry Hill ; 
 and lower down the same stream, another outcrop is met with, whence 
 it can be followed in a north-easterly direction into the adjoining sheet. 
 These crops of the black shales evidently occur along sharp anticlinal 
 folds, such as have already been described in the ground to the west of 
 the Nith. 
 
 Queensberry Group. 
 
 14. This important group of strata covers nearly half the area of the 
 Map. It stretches northwards from the main outcrop of the Lower 
 Black Shales for a distance of thirteen miles, and, as already explained, 
 is easily recognised by its characteristic mode of weathering. A line 
 drawn from Knocknalling on the Ken, north-eastwards by Glen- 
 shimeroch and Troston Hills, Drumloff near Dalwhat, St. Connel's 
 Chapel, to the point where the Scar Water enters the Map, marks the 
 northern limit of this group. In this sheet it is not met with to the 
 north of the great trough of L^pper Black Shales to be described 
 presently. This group contains several horizons, which it is of import- 
 ance to note in detail. At the base of the series and resting on the 
 Lower Black Shales, there is a mass of grey and dark-blue shales and 
 well-bedded flags with occasional grits, which in certain areas reach 
 a considerable thickness. When traced to the south-west, however, 
 this shaly series does not prove a constant zone, for it is found to be 
 split up with thick quartzose grits and sandy flags. This must be 
 borne in mind, as this subdivision does not always reappear with the 
 
13 
 
 black shales, when the latter are brought up by axial folds to the 
 north. This shaly series is probably on the same horizon as the well- 
 known ' Grieston beds ' in Peeblesshire. Above these beds and forming 
 the main feature of the group, there comes a great succession of coarse 
 grits with shaly partings varying from two to ten feet in thickness. 
 These grits are often pebbly, and near the middle of the series they 
 contain some bands of conglomerate. The pebbles vary in size from a 
 pea to half a foot in diameter, and consist of white quartz, quartz 
 rock, blue and grey greywacke, with bits of grey and dark shales like 
 black shales. It is worthy of note that these bands, though placed on 
 the same horizon with the conglomerate of Corsewall Lighthouse, con- 
 tain none of those granite pebbles which are the chief ingredient in 
 the latter. These bands are not traceable for any distance. They 
 shade into pebbly grits with only occasional large pebbles. The surface 
 of the grits is often worn into small- pot-shaped hollows. They are 
 usually of a grey or blue colour, but in some districts the grits as well 
 as the underlying shaly series assume a red or purplish tint. Near the 
 top of the gritty series, there occurs a mass of finely-bedded grey and 
 blue shales, with occasional thin bands of red shales interbedded with 
 the grits, and which are known in this district by the name of the 
 'Barlae shales.' One distinguishing feature of the group is the regular 
 system of jointing which is invariably met with, except in the meta- 
 morphosed areas (par. 31). 
 
 15. The character of the shaly or Grieston series at the base, as well 
 as its relation to the Lower Black Shales and the overlying mass of 
 grits, are well seen in the Scar Burn, which runs into the Old Water, 
 and on the west face of the Steilton HiU north of Newtonaird. After 
 repeated flexures of the overlying grits, the grey and blue shales are 
 again exposed by reason of a south-easterly dip, in the Auchenhay 
 Burn and in the Water of TJrr north of Corsock. To the north of the 
 Barend and Crogo crop of the black shales, the grits rapidly succeed 
 and form a marked synclinal trough, the axis of which extends from 
 Mid Arvie near Loch Ken, north-eastwards by Craighill to the north 
 edge of the Marnhoul Wood. This axial line is about midway between 
 the Lowes crop of black shales to the north and the Barend crop to 
 the south ; and as the dip is tolerably constant for about a mile on both 
 sides from the black shales to the centre of the trough, it is inferred 
 that beds near the top of the series are here exposed. Well-bedded 
 blue and grey shales occupy the middle of this trough, and as these 
 strongly resemble the Barlae beds to the north, they are placed on the 
 same horizon. To the north of the Glenessland black shale crops, the 
 bands of conglomerate are met with on the Castramon Moor, and 
 Knockoure HUI, and also at intervals to the north-east on the same line 
 of strike, above Stewarton, at Straith, and on the Barjarg Moor. The 
 Lowes crop of black .shales just referred to throws off to the north the 
 members of the gritty series which form characteristic features on the 
 crest and south slope of the Blackcraig Ridge. To the west of New 
 Galloway, on both sides of the Ardwell axis previously described (par. 
 10), there occurs a mass of fissile and soft micaceous shales and flags, 
 which have a uniform dip to the north-north-west. In spite of this, how- 
 ever, from the evidence already stated (pars. 10. and 12), they are believed 
 to be repetitions of the same beds. From the Lodge Knowes crop of 
 black shales, these micaceous shales and flaggy beds are traceable 
 northwards to Glenlee Hill, a distance of about two miles ; but when 
 followed south-westwards along the strike to the Dee at Clattering- 
 shaws (Sheet 8), they barely occupy a fourth of this area. It is evident, 
 
14 
 
 then, that we have here the representatives of the shaly or Grieston 
 series at the base of the group spreading across a considerable tract of 
 ground by reason of sharp inverted folds. To the east of the Ken, from 
 Balmaclellan northwards along the valley of the Garpel, coarse grits, 
 with greywackes, flags, and shales, are exposed along the same line of 
 strike as the beds just described. It is highly probable, therefore, that 
 the Ardwell axis has 'nosed out' (par. 10), and has given place to several 
 minor undulations in higher portions of the gritty series. 
 
 Again, the foregoing shaly series may be traced from Gordonston near 
 Dairy, north-eastwards by Lochinvar, Eegland, the Ballinie Burn near 
 Craigdarroch, Terreran, and Maqueston, to the Laight in the Scar Water 
 — a distance of fourteen miles. From the south-easterly dips met with 
 on the Knockman and Corse Hills, as well as the two streams to the 
 east, it is evident that this shaly series is brought to the surface by an 
 anticlinal fold ; but when traced to the north-east and south-west, 
 though occasional south-east dips occur, as in the Ballinie Burn and to 
 the west of Lochinvar, yet the continuance of the axial line cannot be 
 satisfactorily determined. Those perplexing north-west dips recur 
 which seem to indicate rapid inversions of the strata. Near Eegland, 
 as marked on the Map, a band of very dark, almost black, shale crops 
 out, charged with graptolites. These shales are quite unaltered and 
 well bedded, and though in places they resemble the Lower Black 
 Shales, they are really dark-blue in colour. They are placed on the 
 same horizon as the graptolite band of the Grieston series in Peebles- 
 shire. Additional importance is imparted to this series from the- fact 
 that Professor Harkness many years ago discovered a portion of a 
 trilobite in blue shales belonging to it, near the Laight ^ in the Scar 
 Valley ; while a similar ' find ' was obtained in the course of the Geolo- 
 gical Survey by Mr. A. Macconochie, in the Clodderoch Burn about a 
 mile north of Moniaive. In the Scar Valley the Grieston series covers 
 a breadth of two miles extending from the Laight to the streams 
 behind Auchinhessnane ; but this is only an analogous case to that 
 described west of New Galloway, as the beds ' nose out ' rapidly to the 
 north-east. To the north this shaly series throws off the massive grits, 
 and near their northern limit, about three miles from Dairy, occur the 
 well-known Barlae shales, which yielded to Professor Harkness impres- 
 sions of annelids ^ some of which he referred to new species. Similar 
 interesting remains were also met with in the course of the survey. 
 
 16. In estimating the thickness of the Queensberry group of strata, 
 it must be remembered that the shaly or Grieston series .at the base 
 does not retain a uniform thickness over wide areas, for, in certain 
 sections with few flexures, it measures upwards of 2200 feet, and 
 in others thins away to a few hundred feet, passing into coarse 
 grits and flags with occasional bands of shales. The disappearance of 
 the lower shales causes the Queensberry group to appear as a constant 
 succession of massive grits with occasional flags and shales whose total 
 thickness may be estimated at 4500 feet, including 300 feet of flaggy 
 shales at Barlae. 
 
 There are certain detached areas of metamorphism in this group of 
 strata, in which the grits as well as portions of the shaly series assume 
 a different character from that which they usually present. These fall 
 to be described under the Metamorphic rocks. 
 
 17. North of the line indicated in par. 11 as the probable main out- 
 crop of the Lower Black Shales, the area east of the Nith included in the 
 sheet is occupied by the Queensberry group, except where the anticlinal 
 
 ' Vide Appendix. ' Vide Appendix. 
 
15 
 
 folds have brought up the Moffat shales. In the Garroch Burn thin 
 bands of conglomerate occur, which are probably on the same horizon 
 as the bands referred to in par. 15. 
 
 Dalveen Group. 
 
 18. The mass of strata which comes next in order is distinguishable 
 from those just described, by the absence of those thick-bedded grits 
 which are the essential feature of the Queensberry group. It consists 
 of greywacke bands which, as a rule, are much broken by joints, with 
 masses of shales sometimes well bedded but usually gnarled and twisted. 
 Sometimes the series occurs in the form of regular alternations of well- 
 bedded greywackes with shaly partings, while again it is characterised 
 by thick zones of shales separated by thick-bedded greywackes and 
 occasional grits. The band of fine conglomerate or pebbly grit, known 
 by the name of the 'Haggis rock,' which formed such a well-marked 
 horizon in the Lead Hills district, is likewise met with in this area. It 
 has the usual features met with elsewhere, containing small pebbles of 
 quartz, lydian-stone, and jasper. 
 
 19. This group crosses the Map in two parallel bands, the one to the 
 south and the other to the north' of the great synclinal trough. On 
 the south side it is well exposed in the Ken from the Carsfad Holms 
 to Upper Strangassel, dipping steadily to the north-west at an angle 
 of from 70° to 80°. From thence it is traceable in a north-easterly 
 direction, by Cairnyhill, the Corrodow and Castle Camp Hills, to 
 Auchenbrack, where it is overlapped in part by the conglomeratic 
 series of the Caradoc area. From this point to the Brown Hill, at 
 the edge of the sheet, only a portion of the group is visible between 
 the boundary of the Caradoc area and the northern limit of the 
 Queensberry series. The ' Haggis rock ' is seen to advantage in the 
 Ken just below the Blackpark Heugh, and is traceable to the Cleugh 
 Bridge below Liggatcheek. It reappears in the Auchenstroan Crag, 
 at the county boundary near the source of the Stranshalloch Burn. 
 On the east face of the Brown Hill (Sheet 15) it is again caught up, 
 and immediately behind the Breconside farm-house, in the Breconside 
 Burn, as well as near the foot of the Taeholm Burn, it is found to 
 possess its ordinary character, containing small pebbles of quartz, 
 jasper, and lydian-stone. In the Taeholm Burn imperfect traces of 
 encrinites were discovered in this band, in the course of the Geological 
 Survey. This group is well exposed in the Nith near Crairiehill, and 
 again in the railway cuttings from Enterkinfoot close to the margin of 
 the Carron basin. 
 
 20. Rising out from underneath the overlying Lowther series, on 
 the north side of the trough, the members of this group are again dis- 
 played with a marked south-easterly dip, reaching from the mouth of 
 the Polifferie Bum, close to the ring of metamorphosed rocks surround- 
 ing, the Cairnsmore granite, whence it extends eastwards to the 
 Coranbae Hill. In this region the Dalveen beds as well as the 
 overlying Lowther series form a group of well-rounded hills with 
 smooth tops and slopes, while here and there the harder bands 
 protrude. Excellent sections are to be found in the Polifierie Burn 
 as well as in the streams which join the Ken at Carlae. Many 
 of the shale zones are well bedded, but the greywackes and grits 
 are considerably smashed and jointed and traversed by numerous 
 veins of quartz. The thickness of this group is estimated at 3700 
 feet. 
 
16 
 
 Lowther Group. 
 
 21. This series of beds, while succeeding those just described, flanks 
 the two parallel zones of Upper or Lead-Hill Black Shales. Every- 
 where along the margin of the south crop, the members of this series 
 pass underneath the black shale with a marked north-westerly dip, 
 while along the north crop they reappeax with a distinct south-east 
 dip. This series, when typically developed, consists of a great thickness 
 of grey and blue shales and finely laminated flaggy bands, with only 
 occasional thick beds of greywacke and grit. In certain sections, both 
 in this sheet and the one to the north, the grits become pebbly and 
 pass into a fine conglomerate resembling the ' Haggis rock.' There are 
 marked indications, however, of a gradual change in the character of 
 this shaly and flaggy series, along the north side of the trough. Thick 
 grits and greywackes are frequently intercalated with the shales, and 
 massive pebbly beds are of common occurrence. This peculiar feature 
 is also noticeable in the ground to the north of Portpatrick, and is 
 referred to in the Explanation of Sheet 3.^ The section which best 
 displays the normal shaly character occurs in the Ken, from Upper 
 Strangassel to the mouth of the Black Burn, where the beds may be 
 seen (fipping to the north-west at an angle of 70° to 85°, and likewise 
 plunging below the Upper Black Shales. To the west of the junction 
 of the Deugh with the Ken close to the Carsphairn Koad, a lenticular 
 band of conglomerate occurs in the midst of the shales. This series 
 may be traced along the south side of the syncline by the Culmark 
 and Fingland Hills, the Glenjaan Burn, the Ball Hill, to the Appin. 
 In the Glenjaan Burn they roll about, but on the whole they are 
 inclined to the north-west. They are well exposed in quarries on the 
 hill-slope near the mouth of this burn, and close to the roadside near 
 the Caradoc boundary. Here the shales are dark and glossy, and have 
 been used as 'slates.' A band of pebbly grit occurs on the hUl-sIope 
 a little way south of this burn. A thin strip of this series is traceable 
 along the south side of the tongue of Caradoc grits and conglomerates, 
 which stretches westwards to the county boundary. They are to be 
 found in the small streams near Glenjaan and Gorrodow, and when 
 traced eastwards to Cormilligan they seem to be overlapped by the 
 Caradoc grits. 
 
 22. On the north side of the trough this flaggy and shaly series is 
 seen to advantage in the burns at the head of the Dalwhat Water, the 
 ' Appin' Burn, and also in the Auchrae Burn which joins the Ken below 
 Craigengillan. On the slopes of the Benbrack Hill the shales have 
 yielded worm tracks. A well-marked band of fine conglomerate occurs 
 on the crag behind the Oonrick in the Dalwhat Water. From this 
 point westwards, the sandy series above referred to may be traced as 
 a gradually widening zone occupying the Little Dibbin, Manwhill, and 
 Marscalloch Hills. Along this line the greywackes, grits, and shales 
 are baked together as well as much broken by joints. Veinings of 
 quartz traverse the beds in many places. 
 
 It is of importance to note the gradual thickening of this altered 
 sandy series to the south-west, as it throws light on the structure of the 
 Kells and Merrick ranges to the west. Though in this district it is 
 stiU possible to draw a boundary line between the Lowther and Dalveen 
 groups, yet in the high grounds to the west this distinction has been 
 abandoned, owing to the frequent intercalations of masses of grit and 
 
 ' Vide Explan. to Sheet 3, p. 16, where a probable explanation is given of this 
 peculiarity. 
 
17 
 
 greywackes. They have therefore been mapped as one great series, as 
 will be pointed out in the Explanatim to Sheet 8. 
 
 Within the metamorphic area of Cairnsmore of Carsphairn the 
 flaggy Lowther series again appears associated with a band of Upper 
 Black Shales. The beds are still inclined to the south-east. There is 
 here evidently an inversion of the strata, a conclusion which is con- 
 firmed by the evidence obtained in Sheet 8. 
 
 23. Continuous with the two parallel bands of shales and flags 
 above described, the same beds can be traced across Sheet 15, to the 
 Lowther range. Along the north side they are exposed in the Glen- 
 manno and Glenwhargen Bums and on the Glengenny Muir ; while to 
 the south, they are met with in the Druidhall Burn above the Moat, 
 the Breconside, Taeholm and Burn Sands Bums, and in the Nith from 
 Enterkinfoot to Burnmouth. In many of these sections the shaly 
 character of the series is admirably seen, only occasional masses of 
 pebbly grit and bands of conglomerate being intercalated with the 
 shales. A glance at Sheet 15 will show that the synclinal trough of 
 the Upper Black Shales, the axis of which passes through Eliock Wood, 
 is still well marked in the Nith. The Lowther shales pass underneath 
 on the south, only to reappear on the north ; and as these are followed 
 in the direction of the Cairn Hill, to the Auchenloan Bum at the north 
 edge of the Carron basin, their strike becomes more easterly, while the 
 south dip continues. This seems to indicate that the trough is rapidly 
 ' nosing out ' in this direction, so that the Lowther series encloses the 
 black shales of the Lime and Ha' Cleuchs before the Carron basin is 
 reached. As already pointed out in the Explanation to Sheet 15, the 
 Lowther series forms a well-marked trough along the Lowther ridge. 
 The dips prove that the axial line swings round on Thirstane Hill 
 towards the bend in the Auchenloan Burn near Glenim. Here a black 
 shale band crops out, which is traceable westwards by the Long Clench 
 to Dalpedder HiQ ; and similar crops may be seen in the Glenim Burn as 
 marked on the Map. Though it is believed i that along the crest of the 
 ridge the top of the Lowther series is not reached, yet it is highly pro- 
 bable that the trough deepens westwards, allowing a portion of the 
 Upper Black Shale series to succeed. South-east dips occur along the 
 course of the Glenim and Dalpedder band, but in spite of this inversion 
 it is inferred that this crop lies in the trend of the Lowther axis, and 
 that only a portion of the Lowther shales are folded between the 
 Dalpedder bands and those which are met with on the south side of 
 Cairn Hill. The thickness of this group is estimated at 4250 feet. 
 
 Upper or Lead Hill Black Shale Group. 
 
 24 There is a close resemblance between the members of this series 
 and the Lower or Mofiat Shales previously described. It is composed 
 of bands_ of black shales with dark anthracitic flaggy beds, grey 
 shales, with flinty greywackes or beds of chert — the whole series not 
 exceeding 550 feet in thickness. Like the Lower group they are 
 sniashed and twisted to a wonderful degree, and seamed with numerous 
 veinings of quartz. Iron pyrites is very abundant, and occasionally 
 small patches of decomposing anthracitic matter are met with in the 
 heart of the shales, as in the Dibbin Lane. They are rarely well lami- 
 nated, though exceptional instances occur, as near Shinnelhead, where 
 they split in thin laminae. Almost in every section where the bands 
 are exposed they are found to be well charged with graptolites, and in 
 certain places the organic remains are covered over with a thin incrusta- 
 ' Vide Explain, to Sheet 15, p. 12. 
 B 
 
18 
 
 tion of alum. This is specially noticeable in several exposures in the 
 Dibbin Lane. As a rule, where the black shales occur, the flinty ribs 
 or chert beds accompany them. So invariably is this the case, tliat, 
 while mapping out the western prolongations of this series, the appear- 
 ance of the ribs of chert was a sure indication that the black shales 
 were close at hand. 
 
 25. As shown upon the Map, the members of this series cross the 
 north-east corner in two thin parallel lines — the distance between the 
 two varying from half a mile to a mile. The north crop is traceable 
 continuously from Shinnelhead to the county boundary, where it passes 
 underneath a covering of drift, and reappears again west of Manwhill. 
 From Stroanpatrick to the High Bridge of Ken another blank occurs, 
 which may be accounted for by the thick deposit of boulder clay whicb 
 fills the centre of the valley. The same crop is seen in the Deugh 
 above Dalshangan. This thin series, thus traceable over a distance of 
 ten miles, dips below a group of flags, shales, and grits, only to rise again 
 within a short distance, but with a marked inclination to the north- 
 west. As in the former area, there are here likewise numerous blanks, 
 conspicuous amongst these being the one which extends from the 
 Carlae HUl to Stroanfreggan Bum. The reason already assigned 
 partly accounts for some of these instances. It is important to note 
 that these parallel crops do not preserve a uniform distance from each 
 other. The greatest breadth in the Dalwhat Water is about a mile ; 
 but not much more than the same distance to the east, in the Appin 
 Burn and near Shinnelhead, they are repeated by sharp folds, so that 
 the distance between each crop does not exceed much more than a 
 quarter of a mUe. 
 
 These two parallel crops can be followed across the southern portion 
 of Sheet 15. The south zone is traceable without a break to the Nith, 
 and is caught up again near the sources of the streams above Kirkbride ; 
 while that to the north is represented by two lenticular strips extend- 
 ing from Glenmanno to the head of Glenwhern Burn, and again from 
 Glengenny Muir to the Cairn Hill. 
 
 Carsphaim Group. 
 
 26. Eesting conformably on the members of the group just described, 
 and filling the centre of the trough, there succeeds a mass of coarse 
 grey grits, shading into fine conglomerates with greywacke bands and 
 shales. This series attains a remarkable development near the village 
 of Carsphairn in the sheet to the west, whence they take their name. 
 There they are found to lie in small synclinal troughs of the Upper 
 Black Shales, and from the manner in which the bands of black shales 
 are interbedded with bands of grit, it is inferred that the one series 
 succeeds the other without any break. In the course of the Geological 
 Survey, a series of red grits with shaly partings has recently been met 
 with in the Lammermoors, occupying a similar position.^ The latter 
 are, without doubt, the counterparts of the gritty series occurring in 
 this district. From the evidence thus obtained over widely separated 
 areas, it is clear that the beds now referred to are totally distinct from 
 the gritty and conglomeratic series of Caradoc age, in the Lead Hills. 
 
 The best exposure of the present group in this sheet, is met with on 
 the MartouT and Carlae Hills, and in the lower portion of the Benbuie 
 Burn. In the latter section the members of this series rest on the 
 black shales. On the Martour Hill the coarse grits shade into fine 
 
 1 Mr. B. N. Peach has recently mapped corresponding zones of grits along the 
 Lammermoor ridge. 
 
19 
 
 conglomerates in places, containing pebbles of white quartz, lydian- 
 stone, and bits of dark shales like black shales. Where the Upper Black 
 Shales converge or where they are repeated by sharp folds at short 
 intervals, the grits and shales gradually die out. To the north-east, in 
 Sheet 15, the representatives of this series may be traced between the 
 two parallel bands of black shales already referred to. In the course 
 of the survey, certain fragments of fossils were found in a fine grit 
 belonging to this series, in the Lime Cleugh north of Kirkbride ; but 
 these were quite indeterminable. From the dips in the Ken it is 
 apparent that the beds are considerably folded, so that the thickness of 
 strata cannot be great. This conclusion is strengthened by the frequent 
 outcrops of the black shale series in the Appin Burn and near Shinnel- 
 head, the flexures being sharp enough to bring them to the surface. 
 The thickness of the group probably does not exceed 1200 feet. 
 
 Caradoc Beds. 
 
 27. On reference to the Map it will be seen that the Caradoc areaextends 
 from the south slope of Cornharrow Hill eastwards by Glenjaan, Auchen- 
 brack, Arkland Eig, to the Scar Water, where it ' noses out ' on the 
 hill-face east of Chanlockfoot (Sheet 15). The strata included in this 
 area consist, for the most part, of coarse conglomerates which shade 
 into pebbly grits and gritty greywackes with thin shaly partings. The 
 series, as a whole, is conglomeratic, though here and there the con- 
 glomerates abruptly end off, and are represented by coarse grits and 
 greywackes. These conglomerates are exposed in the Scar and Chan- 
 lock Waters near Chanlockfoot (Sheet 15), in the Shinnel Water at 
 Auchenbrack, and in the small streams draining the Countam and 
 Lamb Craigs, as well as on the hill-slopes near Glenjaan. The coarser 
 conglomerates usually occur in the centre of the area, while the finer 
 bands are to be met with near the margin. This gradation is well seen 
 in the Shinnel Water near Auchenbrack. The pebbles are embedded in 
 a hard greyish matrix sometimes calcareous, and vary in size from a 
 pea to a foot in diameter. They consist chiefly of quartz, quartz rock, 
 lydian-stone, blue and grey grey wacke, grey shales, and pieces of black 
 shale. The pebbles are as a rule well rounded. The quartz and quartz 
 rock pebbles predominate, though the fragments of greywacke are also 
 very abundant. As a rule the matrix is extremely tough, so much so 
 that the pebbles can be dislodged while the mass remains intact ; but in 
 some places, as in the March Bum, it decomposes into a brownish earthy 
 gravel. In the Chanlock Water (Sheet 15) the fragments of black 
 shales yielded several graptolites, while near the Lamb Craigs and 
 Glenjaan similar pieces were frequently met with, which also proved 
 fossiHferous. A few fossils have been obtained from some of the bands 
 of conglomerate, which seem to prove that these beds are of the same 
 age as the Caradoc basin of the Lead Hills. The Caradoc beds here 
 referred to, do not lie in a trough of the Upper Black Shale series, as 
 is the case at Duntercleuch and Glendowran in Sheet 15, but rest 
 unconformably on the Lowther Shales, and perhaps on a portion of the 
 Dalveen group. While thus correlating the beds in these two areas, it 
 is important to note the paleontological and physical evidence on which 
 these conclusions are based. In the course of the Geological Survey of 
 the Lead Hills, in*1868, a group of beds was discovered lying in a 
 trough of the Upper Black Shale series. It then appeared, as was sub- 
 sequently pointed out in the Explanation to Sheet 15, that the occurrence 
 of the conglomerates and the apparent overlap of the upper on the 
 
20 
 
 lower strata, indicated the existence of an unconformable junction 
 between tbe Caradoc and Llandeilo rocks.i In this series several 
 bands of conglomerate were found which proved highly fossUiferous. 
 Of the fossils obtained from these bands 41 species were determined by 
 Mr. R. Etheridge, F.H.S. ; 23 species being referable to the Caradoc 
 formation, 19 to the Lower Landovery, and 18 to the Upper Lan- 
 dovery. 
 
 28. Amongst the Brachiopoda from the Lead HiUs is OrtMs 
 Bowhardii, which, according to Mr. Davidson, irrespective of its occur- 
 rence in the Wenlock limestone, is found in the Lower Landovery or 
 Caradoc of Penwhapple Glen, Girvan (Mon. Brack, p. 210). Similarly, 
 Atrypa hemisphcerica (Sow.), is stated by the same author to be ' charac- 
 teristic of the Upper, and to be more rarely found in the Lower 
 Landovery beds.' It is also exceedingly plentiful in the Landovery 
 rocks of the Girvan district (Mon. Brack, p. 139). One fragment of 
 Pentamerus dblongus was doubtfully determined as being present iu the 
 collection. If this species really occurs in the Lead HUls basin, it 
 proves to some extent Lower Landovery affinities. According to Mr. 
 Davidson, this fossil ' would appear to be restricted to the Lower and 
 Upper Landovery rocks, and to be very much more abundant in the 
 last-named formation.' Of the 23 Caradoc forms, a portion of the 
 shield of Trinucleus fimbriatiis was obtained. This species does not 
 appear to range above the Caradoc. Of the Brachiopoda, Leptcena 
 tenuicincta, according to Mr. Davidson, appears to be characteristic of 
 the Caradoc and underlying beds (Mon. Brack, p. 328). Stropkomena 
 grandis occurs chiefly in the Caradoc of the west of England and 
 Wales, and is also found near Girvan {Mon. p. 312). Fragments of an 
 essentially characteristic form, Glyptocrinus? (Ooelocrinus) basalis (M'Coy), 
 occur not less than about 30 times in the collection of 220 specimens ; 
 while the casts known as Petraia about 28 times. From the slight 
 preponderance of Caradoc fossils, the beds belonging to the Lead Hills 
 basin may be considered as of Caradoc age, though it is of importance 
 to note the appreciable number of forms which are characteristic of 
 the Lower and Upper Landovery formations. 
 
 29. In the Caradoc areas to the south-west of the Lead HUls basin, 
 in Sheets 9 and 15, the fossils found were fragmentary and very inde- 
 terminable. Of the seven species obtained, four occur in the Lead Hills 
 basin, amongst them being the characteristic Crinoid, Glyptocrinus basalis. 
 Of the three remaining forms, Stropkomena rkomboidalis was not met 
 with in the Lead Hills conglomerate. It is characteristic of the Caradoc 
 and overlying beds. There is some doubt regarding the identity of the 
 two remaining forms. The first is either Ortkis Bouckardii (Dav.) or 
 Ortkis crispa (M'Coy), but so far as the age of the beds is concerned, 
 this uncertainty is of small moment. As previously stated, Ortkis 
 Bouckardii ranges from Caradoc to Wenlock; whilst Ortkis crispa, 
 according to Mr. Davidson, is chiefly met with in Caradoc beds, and 
 also in Lower Landovery rocks. The remaining form is either Stro- 
 pkomena pecten or Stropkomena retroflexa. The former ranges from the 
 Caradoc to the Wenlock ; while the latter is a Scotch and Irish Caradoc 
 fossU only. 
 
 30. The group of strata from which have been derived the fossils 
 referred to in the foregoing paragraph, rest chiefly on the Lowther 
 Shales series to the south of the great syncUnal' fold. At Wood- 
 end, on the hUl-slope, east of Chanlockfoot (Sheet 15), the finely 
 laminated flags and shales of the Lowther series may be seen dipping 
 
 ■ Vide Explan. to Sheet 15, par. 30, 
 
21 
 
 underneath the coarse conglomerates. At Ridding's Cleuch in the 
 Scar, and in the Chanlock Burn, the members- of the Lowther series 
 roll over to the south-east, and likewise dip underneath the con- 
 glomerates. As the conglomeratic series is traced to the south-west by 
 Arkland Rig and the Lamb Craigs, it overlaps the members of the 
 Lowther group. At this point the conglomerates rest directly on the 
 Dalveen beds, and approach very near to the outcrop of the Queens- 
 berry grits. Near Cormilligan, the basin thins out considerably, and 
 is represented to the south-west by a narrow strip of coarse pebbly 
 greywackes, which pass into coarse conglomerates on Glenskelly Hill 
 and on the hDl-face west of Glenjaan. In the small streams which join 
 the Dalwhat Water between Corrodow and Glenjaan, the dark-blue 
 flags and shales of the Lowther series are seen dipping steadily to the 
 north ; while to the north of the Caradoc area, at Craigenbeast, and in 
 the Glenjaan Bum, members of the same series are met with, which 
 are traceable northwards' till they pass underneath the Upper Black 
 Shale group. The Caradoc beds must ' nose out ' near the county 
 boundary, for the Lowther beds crop out continually from the Fingland 
 Hill to the Stroanfreggan Burn. Further evidence, which seems to 
 strengthen the proof of the uncomformable relation of the Caradoc 
 beds to those which underlie them, is to be found on the north side of 
 the basin, in the valley of the Shinnel. Behind the Appin, and again 
 along the margin of the basin near the course of the Shinnel, the blue 
 flaggy shales of the Lowther series abut against the bands of con- 
 glomerate. At this point the shales dip to the north and are con- 
 siderably crumpled; the relations which the one set of strata bear 
 to the other are, however, distinctly seen. Owing to the want of 
 satisfactory dips, it is impossible to form an accurate estimate of the 
 thickness of the strata contained in this area ; but it is probable that 
 the extreme thickness does not exceed 2000 feet. Still further to the 
 north-east, in Sheet 15, another outlier of fossiliferous conglomerate has 
 been met with. This band is limited in extent and occurs only in two 
 places — ^in the roadside cutting about half a mile south of Burnmouth, 
 and again in the Burnsands Burn about half a mile above Crairieknowe. 
 It rests in a small synclinal fold of the Lowther series. The con- 
 glomerate resembles in general character the finer bands in the valley 
 of the Shinnel, and, viewing this in connection with the fossil contents, 
 it may be considered as of Caradoc age. From the evidence now 
 adduced, there can be little doubt that an unconformity exists between 
 the Caradoc beds and the underlying Llandeilo rocks. In the Lead 
 Hills district, as has already been stated, the fossiliferous conglomerates 
 rest on the Upper Black Shale series ; while in the areas to the south 
 west, they lie partly on the Lowther and partly on the Dalveen groups. 
 It is difficult to determine whether this unconformity is a violent one. 
 The great crumplings and contortions to which both the Caradoc a;nd 
 Llandeilo rocks have been subjected, not only conceal this important 
 fact, but also make it extremely difficult, even with careful and detailed 
 mapping, to detect the very existence of an unconformity. 
 
 Metamorphism of Silurian Areas. 
 
 31. There axe several metamorphic areas included in the sheet. 
 They occur mainly round the granitic centres, but there are also several 
 isolated instances of partial metamorphism apart from any visible mass 
 of igneous rock. In the case of these isolated instances, the rocks have 
 merely undergone a slight alteration without assuming any distinct 
 
22 
 
 crystalline texture. The beds have been considerably hardened, and 
 are traversed with joints in all directions. Occasionally' bands of 
 shales, flags, and greywackes have been so baked together as to form a 
 coherent mass, which is evidently the result of intense compression. 
 Instances of this kind of alteration may be seen on the Stroanpatrick 
 Hill, Manwhill Hill, and eastwards by the Dibbin Lane on the north 
 side of the Upper Black Shale trough. But between New Galloway 
 and Thornhill, the strata exhibit a more advanced stage of meta- 
 morphism. There are detached areas where a distinct schistose texture 
 has been superinduced without any marked crystallization. These 
 schists are often very quartzose and abundantly charged with iron 
 pyrites, which causes them to weather with a dull rusty colour. Here 
 and there dark blotches occur in the rock which resemble the clay galls 
 commonly met with in the unaltered greywackes. The beds are very 
 shattery and much jointed, and are intersected by numerous veins of 
 quartz and calc-spar. These schistose areas are to be met with on the 
 Barmorrow Moor near Balmaclellan, on the Blackcrai^ Hill, and on the 
 Craigneston Hill eastwards to Moniaive. 
 
 32. The metamorphism associated with the granite masses is much 
 more pronounced. As may be seen from the Map, there are three 
 patches of granite, each of which is encircled by a belt of crystalline 
 strata representing different stages of metamorphism. It is worthy of 
 note that these granitic areas occupy different horizons in the Llandeilo 
 rocks ; the Cairnsmore of Carsphairn mass Ipng in the Lowther and 
 Dalveen groups, the Loch Ken area in the Queensberry series, while 
 the narrow strip of Mabie granite occurs among the Ardwell beds. 
 The nature of the metamorphism is determined mainly by the character 
 and composition of the strata in these various groups. The coarser 
 quartzose beds are converted into quartz rock, the thin siliceous 
 shales and flaggy bands into lydian-stone and cherty beds ; while those 
 rocks which contain a considerable proportion of clay mixed with sand 
 have assumed a schistose texture. Instances of the first two kinds 
 of metamorphism are admirably seen in the neighbourhood of the 
 Cairnsmore of Carsphairn mass, and specially on the Moorbroch Gairy. 
 Where the rocks are more felspathic, the alteration extends much 
 farther away from the margin of the granite, than in the quartzose 
 areas. Near the outer limit, the flags and shales begin to assume a 
 crystalline appearance, occasional flakes of mica being scattered through 
 the mass. When these beds are traced towards the granite, they pass 
 into dark-grey spotted schists, in which mica is abundantly 'developed. 
 There are also rude traces of foliation at this stage, which becomes more 
 distinct near the edge of the granite. The dark spots seem to be 
 mainly due to small clusters of brown mica. Along the margin of the 
 granite, the spotted schists pass into perfect mica schists, and in some 
 cases of extreme metamorphism the rock resembles gneiss. The chief 
 ingredients are felspar and mica, arranged in parallel lines, with 
 some quartz, thin veinings of quartz and calc-spar being traceable 
 along the planes of bedding. The foliation and crumpling of the 
 different bands are very distinct. Good instances of this extreme 
 metamorphism are to be found on the Knocknairling Hill west of New 
 Galloway, near the edge of the granite ; while the spotted schists and 
 lydian-stones are well seen in the wood west of Loch Ken. Some of 
 the dark flaggy bands do not assume a schistose texture, but are 
 extremely hard and subcrystalline. On the top, and along the slopes 
 of the Bennan Hill, west of Loch ICen, certain blackish-blue and grey- 
 shales occur in a highly altered condition. They are extremely tough 
 
23 
 
 and abundantly charged with iron pyrites, while the bands are squeezed 
 together in such a way as to form a coherent mass, breaking into blocks 
 several feet square. The well-known granite veins described by Sir 
 James Hall, which shoot out from the main mass on this hill-top, are 
 intruded among these altered shales. They seem to represent the 
 Lower Black Shale series in an advanced stage of metamorphism, 
 as referred to in par. 12. All traces of graptolites are completely 
 destroyed. This conclusion is strengthened by the fact, that on the west 
 side of this tract of granite in the Newton-Stewart district the black 
 shales with graptolites can be traced continuously into the meta- 
 morphic area close to the granite, where they present features which 
 closely resemble those now described. Farther to the north, in the 
 metamorphic ground west of New Galloway, there are two parallel 
 bands of black shales similarly altered, the one close to the New 
 Galloway Eoad and the other extending from Waukmill to the edge of 
 the granite. The shaly and flaggy beds of the Ardwell series north of 
 Mabie, exhibit the various stages of metamorphism already described ; 
 but, in addition to the intense crumpling of the strata, the rocks are 
 often coated with serpentine. Though the gradation in the meta- 
 morphic areas from imperfect crystalline masses to regular mica schists 
 is easily traceable, no instance has been met with of an actual passage 
 from the schist or gneiss into granite. The boundary between the two 
 is generally a well-marked line. The extent of these altered rocks is 
 determined by the nature of the strata, and varies in breadth from a 
 few hundred yards to nearly two miles. It is important to note that 
 the normal strike of the metamorphic rocks are not affected to any 
 great extent by the masses of granite. 
 
 33. At Barnmuir HiU, immediately to the east of Closeburn Castle, 
 there occurs a small detached area where the strata have undergone 
 partial metamorphism. Owing to the thick covering of turf, the passage 
 from the ordinary greywacke into the crystalline-granular rock cannot 
 be seen. The more intensely metamorphosed portions are seen only as 
 Uttle knobs, in the midst of comparatively unaltered greywackes and 
 grits. The Silurian strata, in approaching the metamorphic patches, 
 become harder and show numerous veinings of quartz. The prevailing 
 character of the more altered portions is that of a dull green semi- 
 crystalline mass, weathering into nodular fragments. 
 
 Igneous Eocks in Silurian Areas. 
 
 34. The granite round Cairnsmore of Carsphairn and that to the west 
 of Loch Ken, have much the same lithological character. Near the edge 
 of the former mass, the rock is fine grained and usually grey in colour, 
 while near the centre the crystals of felspar reach a considerable size, a 
 feature specially noticeable on weathered surfaces. The granite of the 
 Loch Ken area is mostly coarse grained, though here and there it 
 shades into bands of pink hornblendic porphyry. The rock consists of 
 white and pink orthoclase and plagioclase felspar, quartz, mica, some 
 hornblende, with a little iron pyrites. Over wide areas, constant litho- 
 logical varieties are to be met with, owing to the presence or absence 
 of the respective minerals. Sometimes the quartz, which is usually 
 very abundant, disappears almost entirely; and again the mica often 
 gives place to hornblende. The Mabie variety differs considerably from 
 the granite of the foregoing areas. The chief constituents are ortho- 
 clase felspar and hornblende, while mica is sparsely developed, and quartz 
 is rarely present. Crystals of sphene are tolerably frequent near Loch- 
 aber Loch. The rock has a distinct foliated texture, which disappears 
 
24 
 
 at some distance from the margin of the granite ; and along with the 
 disappearance of the foliation it is observable that the hornblende is 
 not so abundant, while the quartz and mica increase in quantity. 
 Numerous veins of fine-grained granite and elvanite are to be met with 
 in the heart of the granite areas, while along the margins similar veins 
 traverse the metamorphosed strata. The best examples of the marginal 
 veins occur on the Bennan Hill west of Loch Ken. The white coloured 
 bands alternating with the dark metamorphic schists are so conspicu- 
 ously marked as to be easily recognisable from the New G-alloway 
 Eoad.i The more important veins are connected with the main mass 
 of granite, but in many cases they are lenticular and coinpletely isolated 
 on the surface. They are usually fine grained, and consist of the 
 ordinary ingredients of granite, occasionally passing into a rock made 
 up of felspar, white mica, and a little quartz. They sometimes shade 
 into a rock with a compact grey and pink felspar base, with distinct 
 crystals of hornblende and felspar scattered through it. In the Moor- 
 brock Garry to the east of Caimsmore of Carsphairn, a small isolated 
 patch of granite occurs surrounded by a highly metamorphic zone. 
 Near the edge of the mass the rock is very compact, with a greyish 
 felspar base and some hornblende, while iron pyrites is plentifully 
 developed. Towards the centre of the mass, the rock assumes the 
 character of ordinary granite, being made up of felspar, hornblende, 
 some mica and iron pyrites. A similar patch occurs in the Knocknair- 
 ling Burn, about a mile west of New Galloway, a section which is seen 
 at the roadside above Achie. 
 
 35. Eound the margin of the granite there is often a remarkable 
 development of dykes, which seem to be connected with the granitic 
 centres, though differing considerably in lithological character from true 
 granite veins. The best examples are to be found on the Marthrown 
 Hill north of the Mabie mass, and on the Moorbrock HUl east of the 
 Caimsmore mass. These dykes consist usually of felstone, with a pink 
 and grey felspar base, along with hornblende ; but in some cases the 
 mica is equally abundant with the hornblende. 
 
 36. Outside the limits of the metamorphic areas, there are abundant 
 instances of intrusive dykes among the Silurian rocks, which are totally 
 distinct in their origin from those referred to in the foregoing para- 
 graph. In this sheet there are a few conspicuous examples of dykes 
 cutting across the strike of the beds ; but these are exceptional, the 
 prevaUing direction being along the lines of bedding. They commonly 
 occur in groups, and are abundantly 'associated with the black shales 
 of the Mofi'at and Upper Black Shales series. These rocks may be 
 classified in three divisions, viz. felstones, syenites, and diorites. The 
 felstone type, which is by far the most numerous, has an orthoclase 
 felspar base of a greyish or pink tint, with occasional hornblende 
 crystals, and some free quartz. In some of the dykes iron pyrites is 
 very plentiful, while talc is sometimes met with, as in the dyke at 
 Three Crofts west of Lochrutton Loch. Instances of this class are to be 
 found on Mochrum Fell, at Kirkconnell, in the Auchenhay and Barend 
 Bums, and at Dalmacallan. The syenite type has also an orthoclase 
 felspar base, with some plagioclase crystals and a great abundance of 
 hornblende. The best examples occur near the Bogrie, at the 
 Shirmers, and on the Beuchan Moor. When these rocks are examined 
 
 ^ These veins have long been known from the description given hy Sir James Hall. 
 From the occurrence of these veins he inferred that the granite was more recent than 
 the schists, and had been intruded amongst them in a molten state, thus confirming 
 the generalizations of his Mend Hutton. Vide Appendix. 
 
25 
 
 under the microscope, other minerals may be detected in small quantities, 
 the most conspicuous amongst these being quartz, mica, talc, iron 
 pyrites, along with some calcite. The third type consists of felspar, 
 which seems to be mainly plagioclase, and hornblende. The felspars 
 in several instances are beautifully striated. In some of these dykes, 
 the hornblende is more abundant than the felspar. As in the former 
 types, iron pyrites, a little talc, some calcite, and certain needle-shaped 
 crystals of apatite, are associated with the main ingredients. As 
 a rule, these dioritic rocks decompose very readily and weather 
 spheroidaUy. The best examples of this type occur on the Benbrack 
 Hill north of Moniaive, at Craigengillan, on the Auohenhay Hill, and 
 near Shawbrae west of Dumfries. 
 
 Carboniferous and Permian Bocks. 
 I— Thomhill Basin. 
 
 37. In the Explanation of Sheet 15, a brief description was given of 
 the northern part of the remarkable hollow among the Silurian hills, 
 which has been called the Thornhill basin. Traversed by the valley of 
 the Nith, it might be regarded merely as an expansion of a part of 
 that valley. But that it existed as a hollow long before the present 
 surface configuration of the district was determined, is proved by the 
 nature and position of the strata which occupy its area. As shown 
 upon Sheet 15, the Kith enters it not at its true end, but from the west 
 side a httle above Drumlanrig ; whUe the ancient hollow, quitting the 
 present course of the river, penetrates almost to the base of the Lowther 
 HUls, being prolonged in a deep narrow valley shut in by smooth and 
 steep slopes. Its southern extremity is formed by a closing in of the 
 hills on either bank of the Nith, which escapes through the defile of 
 Blackwood. 
 
 38. This curious and very ancient hollow is only one of a serious 
 by which the Silurian uplands of the south of Scotland are marked. 
 Along the depression traversed by the Nith, three of these occur. One, 
 occupied by the coal-basin of Sanquhar, is bounded by steep Silurian 
 hUls, through which the river escapes by the picturesque gorge between 
 Grange and the Drumlanrig Woods. A little farther south lies the 
 basin of Thornhill ; and about four miles farther on, after working its 
 way through the hills by a narrow outlet, the river enters the broad 
 plain of the Dumfries basin. In the course of the River Annan and 
 some of its tributaries similar ancient hollows occur; while, much farther 
 to the east, other traces of very old basins and valleys are found among 
 the Lammermoor HUls. In some of these cases there is distinct evidence 
 that the hoUows are as ancient as the time of the Upper Old Eed Sand- 
 stone, which occupies their bottoms. In other examples, like those in 
 Annandale, only Permian strata occur, though the hollows may never- 
 theless be as old as the others. 
 
 39. The Thornhill basin was already in existence when the red 
 strata at the base of the Carboniferous system were laid down. It 
 appears to be an eroded hollow, and, from the narrowness of the Black- 
 wood gorge below, as well as the way in which the underlying Silurian 
 rocks come up to the surface, there is reason to believe that the bottom 
 of the hollow under the red rocks is lower than its outlet. It would 
 thus be a rock-basin of palaeozoic date lying on the Silurian rocks. 
 Two other small basins, perhaps at one time connected with that of 
 Thomhill, lie a little to the east, in the parish of Closeburn. 
 
26 
 
 40. Taking the basin as defined by the margin of the rocks which 
 cover its bottom, it has an extreme length from north to south of 
 eleven miles, while its greatest breadth is nearly five miles. Within 
 this area the rocks are arranged in the following descending order : — 
 
 (Briek-red Sandstones -with occasional red shales and clays. 
 Brick-red Sandstones fuU of volcanic debris and bands of red 
 volcanic tufif. 
 Beds of Porphyxite witli tuff and seams of red sandstone inter- 
 stratified. 
 I Sandstones, reddish-grey, red, and white ; with red, purple, and 
 Carhoniferous ) mottled shales and clays. 
 
 ' 1 Red Limestone bands with Carboniferous Limestone fossils. 
 ( Red and reddish-grey Sandstones and Shales. 
 q;i„^;o„ S Greywacke, Grit and Shale, part of the great Lower Silurian region 
 
 suunan, . j of the south of Scotland. 
 
 The Silurian strata have already been sufficiently described in the 
 previous pages. They are here covered unconformably by all forma- 
 tions of youngier date. 
 
 1. Carboniferous Rocks. 
 
 41. Strata belonging to this part of the series of geological formations 
 are shown by the Map to form a rim or band round the basin, con- 
 tinuous on the west side but interrupted on the east by the occasional 
 overlap of the red succeeding rocks upon the underlying Silurian 
 series. As fossils of undoubtedly characteristic Carboniferous Lime- 
 stone species occur among the limestones, it might readily be supposed 
 that there can be no doubt as to the geological horizon of these lime- 
 stones and the sandstones among which they occur. But that these 
 rocks lie far below the base of the true Carboniferous Limestone, cannot 
 be doubted. They exactly resemble the red strata of the lower group 
 of the Calciferous Sandstones of Ayrshire and the rest of the south of 
 Scotland ; while, on the other hand, they can be easily distinguished 
 from the Carboniferous Limestone series. Yet this series comes down 
 the valley of the Nith to within a distance of three miles from the 
 Thornhill basin, retaining its usual character and presenting a marked 
 contrast to the red rocks now under description. Were it not for the 
 fossils of the limestones, no one would hesitate to class the lower 
 sandstones of Thornhill with the basement group of the Calciferous 
 Sandstones. If it can be shown that similar fossils, supposed to mark 
 the Carboniferous Limestone, occur elsewhere among the Calciferous 
 Sandstones,-^that is, below the base of the Carboniferous Limestone, — 
 the position of the Thornhill strata may be established. 
 
 42. In the island of Arran a thick red limestone occurs at Corrie, 
 under many hundred feet of red sandstones, forming the lower division 
 of the Calciferous series. This limestone is full of characteristic 
 Carboniferous Limestone fossUs ; yet it certainly lies far below the 
 base of the Carboniferous Limestone, for it is lower even than the 
 intervening cement-stone group. Again, nearer to the Thornhill area, 
 a copious development of the cement-stone group occurs between the 
 mouth of the Nith, Canobie, and Liddesdale ; and among these strata 
 lie some massive bands of red limestone charged with the characteristic 
 corals, crinoids, brachiopods, and cephalopods of the true Carboniferous 
 Limestone, yet overlaid by masses of sandstone and shale which are 
 lower than the base of the Carboniferous Limestone of Cumberland. 
 It is evident that the abundant fauna of the Carboniferous Limestone 
 series had already been in existence outside our area long before the 
 
27 
 
 limestone series began to be deposited, and while the red sandstones 
 at the base of the Carboniferous system were elsewhere m course ot 
 formation. The conditions under which these sandstones accumulated 
 seem to have been singularly unfavourable to life ; for, on the whole, 
 the rocks are barren of organic remains. At intervals, however, the 
 isolated waters had their barriers so far broken as to allow the open 
 sea outside to enter and iill them, and to bring thither its own 
 characteristic fauna. Such intervals were succeeded by a renewed 
 barring-back of the clear sea, and a return to the previous uncon- 
 genial conditions. The corals, crinoids, and shells were, consequently, 
 destroyed amid the growing deposits of sand and mud. This appears 
 to be the history of the Corrie Limestone, and a similar series of changes 
 seem to have taken place during the formation of the thick limestones 
 in the south of Dumfriesshire and Koxburghshire.i 
 
 43. On these grounds the Carboniferous rocks of Thomhill, though 
 containing limestones with undoubted Carboniferous Limestone fossils, 
 are regarded as older than any portion of the true Carboniferous Lime- 
 stone, and as lying in the same position as the Calciferous Sandstone 
 series of other districts where thick marine limestones are similarly 
 intercalated. 
 
 ■44. Good sections of the red sandstones which form the greater part 
 of the Carboniferous rocks of this district, occur along the western side 
 of the basin, in the courses of some of the streams which descend from 
 the Silurian high grounds into the Nith, as well as in several quarries. 
 The most continuous exposures are to be found at the north end, in the 
 Enterkine Valley. There the sandstones and lilac or mottled clays and 
 shales may be observed, in at least two places, resting upon the vertical 
 or highly inclined and contorted Silurian shales. The latter being 
 there of a pale lilac colour, the Carboniferous clays which were made 
 from their waste have the same colour, and can hardly at first sight 
 be distinguished from them. The upper rocks, however, besides their 
 much less inclination, contain distinct rootlets and other plant remains. 
 Continuing down the Enterkine Valley, they form its eastern side and 
 reach a thickness of about 500 feet. They are covered by an overlying 
 mass of porphyrite of Permian age, which forms the crest and eastern 
 slope of the ridge between the valleys of the Enterkine and the Carron. 
 At the north end of the Drumlanrig Tunnel they are again well exposed 
 in the railway cutting, likewise in some quarries on the east side of 
 the line, as weU as in the AuchenmuUeran Bum which flows past the 
 quarries to the Nith. The dip of the beds is here easterly, at angles 
 varying from 35° in the bum to not more than 10° or 15° at the 
 railway. The Silurian greywacke and shale are also seen in the 
 railway cutting within a few yards from the sandstones, but the actual 
 junction is now obscured. 
 
 45. From this point the boundary line of the basin, sweeping south- 
 ward along the hUl-slopes, strikes the Eiver Nith at the mouth of the 
 picturesque gorge of Duncan's Linn. Here Silurian rocks on the right 
 bank dip nearly due north at an angle of about 50°, while the Car- 
 boniferous sandstones, shales, and clays, forming a ledge on the left 
 bank, dip east by south at 10°. These latter strata contain Stigmaria 
 and other plant remains. They extend down the same side of the 
 river, which they cross at the Mermaid's Stone, and thence range in 
 a southerly direction through the grounds of Drumlanrig, being well 
 exposed along the east side of the river, particularly in a high cliff-section 
 
 ' The red colour of the latter strata may possibly he due in part to the percolation 
 of iron-oxide from a former covering of red Permian sandstone. 
 
28 
 
 below the bridge. In the ravine of the Starn Burn, to the south of 
 the castle, the peculiar hard white, pink, red or lUae, and mottled clays 
 of the lower part of the Carboniferous series have been laid open along 
 the east bank ; while the red Silurian greywacke lies in the bed of the 
 stream below, and ascends the western bank. 
 
 46. From the grounds of Eccles, where the Silurian and Carboniferous 
 rocks are both to be seen, the boundary line between these formations 
 ranges by the east side of Penpont along the foot of the slopes that 
 rise above Keir and Porterstown until it strikes the Nith a little below 
 Barjarg. The best exposure of the Carboniferous rocks in this part of 
 their course, is that in the Barjarg Lime Quarries. The strata there dip 
 gently towards the north-east away from the Silurian hills behind them. 
 The limestone here quarried is the same as the Hmestone of Close- 
 burn to be immediately described. Owing to the depth of 'cover,' 
 it is not now worked open-cast, but by mining, 
 
 47. Along the eastern margin of the basin, the Carboniferous belt is 
 in great measure concealed by the overlap of the Permian series. On 
 the left bank of the Nith, opposite to Barjarg, a marked ridge runs 
 northward to near the village of Closebum. At its southern end it 
 consists of Silurian rocks, but below the farm of Kirkpatrickhill it 
 begins to be covered with a coating of Carboniferous sandstones which 
 appear to continue along the rest of its course to the north, for they 
 are found at the extreme point of the ridge near Closeburn. Its base 
 is bordered by the Permian sandstones, which here completely overlap 
 the Carboniferous series and abut against the Silurian. On the east 
 side of the ridge, the Carboniferous rocks occupy a bay in the Silurian 
 bUls, and here they are marked by containing a considerable mass of 
 limestone, which has long been quarried at Closeburn. Two main 
 seams occur, as shown in the subjoined section : — 
 
 Feet. 
 Eed shaly sandstone and purple and red mottled shales. 
 Red magnesian limestone, ....... 14 
 
 Eed sandstones and clays, 18 
 
 Thick red limestone 18 
 
 48. The upper seam is a magnesian limestone, containing, according 
 to the analysis of Dr. Murray, 42 per cent, of carbonate of magnesia 
 and 54 per cent, of carbonate of Kme. The lower seam, is a tolerably 
 pure limestone, containing 91 per cent, of carbonate of lime, but is 
 seamed with layers of red shale.i The occurence of magnesian lime- 
 stone in association with the red limestone of Closeburn, is another 
 feature which connects these strata with the series at Corrie in Arran, — 
 a red magnesian limestone being there also found above the fossUiferous 
 limestone. 
 
 49. The fossils yielded by the limestone and the shales connected 
 with it, are ordinary Carboniferous Limestone species. The Productus 
 giganteus is particularly abundant here, as it is also in the red Umestone 
 of Arran. But the fossil list is a meagre one, and the specimens 
 are in many cases so badly preserved, that their identification cannot 
 be made with certainty. At present, therefore, no very satisfactory 
 palseontologicaJ comparisons can be drawn between the Closeburn 
 strata and other parts of the Carboniferous system. 
 
 50. Below the Closeburn limestones no Carboniferous rocks come to 
 the surface, the bottom of the valley being covered up with gravel 
 and alluvium. There cannot be a great thickness of rock between the 
 limestones and the underlying Silurian strata. At the lower quarry 
 
 1 Menteith's Geohgy of Dumfriesshire. Edin. New Phil. Jou/mal, 1828, p. 45. 
 
29 
 
 the strata dip to the north away from the older rocks, but at the upper 
 auarrv they are gently inclined to the north-east in such a manner that 
 they dip towards the Silurian hills which now circle round and rise in 
 front of them. Such an arrangement naturally suggests the existence 
 of a fault between the upper quarry and the Sdurian hill of Barmuir. 
 But the red sandstones and shales overlying the hmestones may be 
 traced up to within a short distance from the greywacke, being there 
 flat and quite undisturbed. The dislocation, therefore, if it exists, can 
 hardly be a large one. Again, from the way in which the hmestone 
 bands strike southwards at the Silurian grounds between ^rkpatrick 
 and Upper Eig, it may be inferred that another small fault here 
 separates the two series of rocks. What appears to be a Uttle outlier 
 of the Carboniferous Sandstone, however, occurs on the slope of the 
 hill to the west of Upper Eig. . 
 
 51. A little to the north of Closeburn Castle, the Permian sandstones 
 are found within a few yards from the greywacke, so that the Car- 
 boniferous series is here again overlapped. The Silurian rocks run out 
 into a promontory, which extends from Closeburn to the Cample Water 
 between Cample Mill and Closeburn Mill. The stream has cut a 
 section through both the Carboniferous and Silurian beds, the latter 
 forming the bed of the watercourse, the former rising along the north 
 bank. At one point the unconformable junction of the two formations 
 is exposed. The red and reddish-grey sandstones, sometimes very 
 coarse and even conglomeratic, extend up the Cample for nearly a mile, 
 and are again found in the Crichope Burn near Dollard. _ Here and 
 there they contain red and purple shales with plant remains, the dip 
 of the whole series being toward the north-east at angles ranging from 
 8° to 15°. For a considerable part of the way they are concealed 
 under drift and alluvium, but, if their average dip be taken at 10° 
 and no fault of consequence intervene, there must be here a thick- 
 ness of nearly 700 feet of Carboniferous strata. At their upper end 
 they are overlapped by the brick-red Permian sandstones, the actual 
 junction being visible along the right bank of the Crichope a little way 
 below Burley's Leap. The brick-red hue of the upper formation, 
 distinctly marks it off from the dark-red and purple tints of the forma- 
 tion on which it lies. The unconformity of the two series, however, is 
 not so clearly marked in the cliff section, though it is indicated by the 
 discrepancies of dip. The Carboniferous beds where their inclination 
 can be measured, here dip up the stream, that is, north-north-east, at 
 an angle of 12°. The Permian sandstones so abound in false-bedding 
 that it is often difficult to ascertain their inclination ; indeed they are 
 for the most part quite flat. At the locality now referred to, they 
 seem to dip gently towards the north-west, though this may be 
 deceptive ; and their position in the Crichope Glen is, on the whole, 
 horizontal. 
 
 52. The portion of Carboniferous rocks now under description, lies 
 in a bay of the Silurian rocks, as will be seen by reference to the Map. 
 They dip at low angles away from the older formation, sweeping round 
 by Dressertland, Townbum Wood, Heathery Dam, and Dollard HUl, 
 back along the Silurian slopes to the Crichope Burn. At one point 
 about half a mile to the north-east of the Heathery Dam, they contain 
 a bed of red sandy limestone full of small crinoidal stems. This 
 stratum dips to the north-west at 8° to 10°, and rests almost directly on 
 the Silurian rocks. Probably it is on the same horizon as the Close- 
 bum seams. 
 
 53. It will be observed that the limestones are confined to the 
 
30 
 
 southern end df the basin. No limestone has been observed north of 
 the point just named on the east side, or north of Porterstown on the 
 west side. 
 
 54. On the Orichope Burn immediately below the wood at the Grey 
 Mare's Tail, the Carboniferous rocks disappear, their place being taken 
 by the porphyrite and sandstones of the Permian series. From the 
 want of sections it is not possible at present to determine whether any 
 fault occurs at this place, or whether the Permian series overlaps the 
 Carboniferous here as in other parts of the basin. 
 
 55. For more than a mile to the north, the Carboniferous sandstones 
 do not come to the surface. At a little bay in the Silurian hills behind 
 Townhead, they reappear from under the Permian sandstone, and dip 
 to the south-west at 8° to 10°. They are again lost, and do not crop up 
 untU we reach the hiUside to the east of Morton Castle. Thence they 
 can be traced round the hill on which the farm-steading of Morton 
 Mains stands, westward by King's Quarry to the mouth of the Carron- 
 hill Glen. They appear then to range south-eastwards, forming the 
 rising ground which slopes up from the line of railway into Morton 
 Moor, and reaching again the Cample Water between Windyholm 
 Crook and Newton High Quarry. This portion of the Carboniferous 
 series, as shown on the Map, projects far into the Permian area. 
 
 56. North from Morton Mains the Permian rocks lie next the Silurian 
 hiUs, but three-quarters of a mile beyond East Morton, where they 
 retire a little from the base of the hUls, the characteristic purple shales 
 of the Carboniferous series, with plant remains, appear at the surface. 
 These are speedily overlapped again, however, by the porphyrite, which 
 here circles back and creeps a little up the flank of the Silurian hills. 
 No further trace of the older formation appears along the margin of 
 the basin, untU, after passing Durrisdeer, we find the Carboniferous 
 sandstones exposed by the denudation of the overlying volcanic masses 
 at the upper part of the Colton Burn above Durrisdeer MiU. The sand- 
 stones have here been quarried for fences. This is the most northerly 
 portion of the Carboniferous series to be seen along the eastern margin 
 of the basin. 
 
 57. In addition to the larger Carboniferous area to the east of 
 Carronbridge, three smaller tracts of the same rocks rise within the 
 Permian district. Their appearance is due to the denudation of anti- 
 clinal folds or minor undulatioiis of the lower portions of the Permian 
 series. The most northerly lies a little to the south of Nether Dalveen, 
 where some red and purple sandstone and shale occur on the left bank 
 of the Carron Water. The next is seen along both banks of the same 
 stream between Drumcruilton and Carronbank, rising from under the 
 Permian igneous rocks. The third lies a little way farther down the 
 stream, between Carronbank and the railway viaduct. Eising out 
 from beneath the porphyrite on the north and east sides, it is cut off 
 towards the south by a fault which brings down the brick-red sand- 
 stones against the dull-red sandstones and shales of the Carboniferous 
 series, thus throwing out at this point all the igneous portion of the 
 Permian group. 
 
 58. That the Carboniferous rocks once extended considerably beyond 
 the present limits of the Thomhill basin, is shown by the occurrence of 
 several scattered outliers to the east of the valley of the Nith. One of 
 these lies in the marshy hollow of the Townfoot Loch. Owing to the 
 nature of the surface, no satisfactory sections are obtainable. But 
 traces of the usual purplish-grey sandstone occur, and also, at the south 
 end of the outlier, of an impure siliceous limestone. Another small 
 
31 
 
 Caxboniferous basin lies further to the north, but beyond the limits of 
 this Map. A third detached exposure of the Carboniferous rocks 
 occurs considerably to the east in the Garrooh Valley. It is described 
 in par. 68, together with the Permian strata which overlie it. 
 
 2. Permian. 
 
 59. Above the Carboniferous rocks of the Thomhill basin lies a 
 group of strata consisting chiefly of brick-red sandstones. These are 
 plainly the same as those which extend up the Nith from Annan by 
 Dumfries to Friar's Carse, and form a continuation of the well-recog- 
 nised Permian series of Cumberland. They are also identical in litho- 
 logical character with the red sandstone series which overlies the 
 Upper Coal Measures in Ayrshire, and in which, as in the Thomhill 
 basin, they have at their base an intercalated series of igneous rocks. ^ 
 As shown in the table given in par. 40, they may be grouped in two 
 zones — a lower volcanic series, and a thick overlying mass of brick-red 
 sandstone. 
 
 a. Volcanic Group. 
 
 60. The base of the Permian series in the northern half of the 
 Thomhill basin, consists of a succession of beds of porphyrite. These 
 are not intrusive sheets, but, from their internal character, their associa- 
 tion with bands of tuff, and their occasional interstratification with 
 the sandstones, are undoubetly lavarstreams contemporaneous with the 
 formation df the Permian rocks of this district. Lying at the bottom 
 of the Permian series, they form between that series and the under- 
 lying Carboniferous strata a belt which throughout most of the ground 
 rises to the surface as a distinct ridge. At the north end of the basin 
 it slopes up from the valley of the Enterkine, and running southward 
 as a dividing ridge between that valley and the Caxron Water, retains 
 its greater elevation untU it sinks into the Nith between Dmmlanrig 
 Castle and Carronbridge. On the other side of the basin its influence 
 on the surface is less decided. From Nether Dalveen the volcanic 
 band rises along the east side to form a range of swelling slopes 
 with occasional minor- hillocks as far south as the farm of Gateslack. 
 A little further south it crosses the valley from side to side, so that 
 the red sandstones to the north of the barrier are encircled by it and 
 form a small detached trough. Traced still southward on the eastern 
 side, the porphyrite, like the Carboniferous sandstones below it, appears 
 only now and again between the brick-red sandstones and the Silurian 
 hills. A considerable mass covers the Carboniferous rocks at Morton 
 Castle, whence it stretches south-eastward to the Cample Water, dip- 
 ping eastward under the red sandstones as usual, and rising from 
 beneath them in one or two places along the flanks of the Silurian hills, 
 so as to form here a second minor trough. It is seen, for example, a 
 little to the south-east of Townfoot, and again on the Crichope Burn at 
 the outer edge of the wood that encloses the Grey Mare's Tail. The 
 latter^ locality is the farthest point to which it has been traced on the 
 east side of the basin. On the west side it is seen in the bed of the 
 Nith, below Cairnpark near Drumlanrig, in one or two places on the 
 edge or in the channel of the river nearly as far as Nithbank, and on 
 
 ' See Geological Magazine for June 1866, where volcanic rocks of Permian age in 
 Britain were first described, and where the identity of the Ayrshire and Nithsdale 
 series was pointed Out. 
 
32 
 
 the sloping banks from Tibbers Castle to Burnhead, where it was 
 pierced in sinking a well. It has not been observed to the south of 
 that point. In the southern part of the basin the brick-red sandstones 
 rest directly upon the Carboniferous or SUurian rocks without the 
 intervention of any volcanic zone. 
 
 61. As no detailed account has yet been given of the volcanic rocks 
 of this district, the reference in the Explanation to Sheet 15 of the 
 Geological Survey having been purposely limited, a more particular 
 description of them is desirable in the present publication. 
 
 The porphyrite retains throughout its course a common type of 
 lithological character which is identical with that of the Permian 
 volcanic rocks of Ayrshire. It is a dull purple or purplish-grey por- 
 phyrite, passing from a finely crystalline compact to a dull earthy 
 amygdaloidal or rough vesicular and scoriaceous rock. It appears to 
 consist essentially of a crystalline basis of plagioclase felspar, through 
 which is diffused much haematite, usually in the form of irregular 
 shreds and angular fragments, but sometimes in crystals. The iron 
 has often become hydrous, and sometimes in this condition appears 
 to be pseudomorphic after augite or other minerals. In the fresh 
 crystalline parts of the rock the iron assumes somewhat of the brilliant 
 metallic lustre and red streak of specular iron, but where the rock is 
 more decayed it takes a dull-red colour, and often occurs so abundantly 
 as to give a distinct red tint to the rock. In these circumstances it is 
 soft, fragile, has a blood-red streak, and is almost entirely soluble in 
 boUing hydjochloric acid. In some crystalline portions of the por- 
 phyrite, augite crystals appear conspicuously ; but they are often absent 
 altogether. Olivine and magnetic iron likewise fall, or at least are 
 rare. Most of the rock is much decomposed. Where amygdaloidal, 
 the cavities are usually filled with steatite or other magnesian sihcate, 
 the result, perhaps, of the alteration of the augite. 
 
 62. It may be most advantageous to describe — first, one or two 
 sections where the bottom of the porphyrite can be seen ; then some of 
 those illustrative of its central portions ; and lastly, some good exposures 
 of its upper surface revealing the manner in which it is related to the 
 rocks that overlie it. 
 
 63. At the bend of the Nith already referred to, between Drum- 
 lanrig and Carronbridge, under a wooded bank called the Castle Hill, a 
 good section is seen of the actual junction of the porphyrite upon the 
 Carboniferous sandstones and shales. The porphyrite has the usual 
 purplish-grey hue and finely crystalline tejcture, with abundance of the 
 red mineral. The bottom is in large rough spheroidal masses, having 
 a slaggy appearance where the amygdaloidal cavities have been emptied 
 by the weather. A little higher up, the rock assumes a rudely bedded 
 appearance. It dips eastward, like the sandstones on which it rests. 
 No unconformability between the two could be made out from this 
 section. Another excellent exposure of the junction of the lower parts 
 of the volcanic band with the Carboniferous strata below, is laid bare 
 on the left bank of the Cample Water, about half-way between Gate- 
 lawbridge and Kettleton Bridge, where a steep bank of rock has been 
 cut through by a small stream and cascade. The upper part of the 
 section is formed of the porphyrite, the lower consists of dull-red clays 
 and sandstones. Lying here in apparently conformable sequence upon 
 the beds below, the volcanic mass is separated into different beds, 
 between which there occasionally appear thin seams of brick-red sand- 
 stone fuU of small porphjrrite lapilli. This is an important fact, for 
 the identity of these sandy seams in the heart of the volcanic band 
 
33 
 
 with those in the sandstone above it shows the whole to form part of 
 one connected series. 
 
 64. Several streams have cut good sections across the series ot 
 porphyrite beds. One of these is to be seen in the Cample Water 
 above the section last described. At the north end of Windholm, in 
 particular, a rough amygdaloidal bed dips under a very conipact close- 
 grained rock approaching even to a basalt in the fineness of its texture. 
 This latter bed is remarkable for showing a rudely columnar structure, 
 the only example of the kind which has been met with among these 
 Permian igneous rocks. The columns are not regularly defined, but 
 starch-like, shading into and growing out of each other. The existence 
 of successive lava-flows in this volcanic zone, could not be more clearly 
 shown than by this section. In the Hapland Burn, about half a mile 
 south of Durrisdeer, an excellent cross-section has been cut through the 
 whole of the porphyrite series from bottom to top. A little knob of 
 the rook protrudes to the surface close to the Silurian boundary. This 
 is immediately overlaid by the brick-red sandstones, which dip at a 
 scarcely appreciable angle away from the hills. These sandstones 
 contain pebbles of the igneous rock, and in some beds pass into a kind 
 of sandy and gravelly tuff. They at length dip under the main mass 
 of porphyrite. In this section, therefore, we see that the latter is 
 fairly included within the brick-red sandstone series. If, indeed, 
 beginning on the slopes between Oastlehill and Durrisdeer, we proceed 
 to trace the rocks southward, we discover that some sandstone begins 
 to appear in the porphyrite below the church of Durrisdeer ; and that 
 while the portion of the latter rock overlying this sandstone dies out 
 southward so as not to appear south of Gateslack, the sandstones, in a 
 corresponding manner, swell out until, on the cessation of the porphyrite, 
 they coalesce with the strata which covered it. But the igneous sheet 
 under this sandstone intercalation continues to hold its course along 
 the margin of the basin, appearing there at intervals, as already described. 
 The section in the Hapland Burn exposes a succession of compact and 
 amygdaloidal beds of porphyrite with the usual characters. The 
 Carron Water exhibits some good sections of this series between the 
 railway viaduct and Drumcruilton Cottages. The rocks may likewise 
 be seen to advantage in numerous openings along the chain of ridges 
 which they form between the Carron Water and the Enterkine, from 
 Nether Dalveen as far indeed as their termination along the bank of 
 the Nith west of Thornhill. 
 
 65. The upper surface of igneous beds is exposed in several places 
 on the Carron Water. A few yards below the junction of the Gate- 
 slack Bum with that stream, the porphyrite dips below a dull-red 
 sandy tuff. At Durrisdeer Mill it is again seen in a similar position. 
 But the course of the Carron Water shows the best section in the 
 district of these overlying strata. 
 
 66. Over the sheets of porphyrite now described, comes a group of 
 stratified rocks, consisting essentially of the ordinary Permian brick- 
 red sandstone, but which in its lower portion contains an abundant 
 intermixture of tuff and fragments of porphyrite, either aggregated 
 into distinct lenticular seams or scattered more or less abundantly 
 through the body of the sandstone. That these intercalations were 
 not merely derived from the waste of the older lavas by ordinary 
 mechanical attrition, but point to the continued ejection from volcanic 
 orifices of dust, lapilli, and scoriaceous bombs, is sufficiently plain from 
 many sections to be seen throughout the district. Thus, on the left 
 bank of the Cample Water, immediately to the south of the junction of 
 
 C 
 
34 
 
 the porphyrite mth the Carboniferous strata, an instructive section 
 occurs in which beds of tuif and ashy sandstone run for some way along 
 the face of the grassy bank. One of the tuff beds is a coarse brecciated 
 rock, full of angular and rounded fragments of porphyrite, some of 
 which are rough and scoriaceous like the slags of a modern volcano. 
 The vesicles have been drawn out round the exterior of some of these 
 stones, as round recent volcanic bombs. Layers of the ordinary brick- 
 red sandstone run in and out along the length of the coarse tuff. To 
 the east of Gateslack, some good sections occur of a similar very coarse 
 volcanic agglomerate. Indeed the rock may be seen in almost every 
 stream which, has cut well down into the base of the red sandstone 
 series. 
 
 67. The Carron Water traverses the centre of the volcanic part of 
 the Permian basin of Thornhill, and has exposed a series of admirable 
 sections. The lower reaches of this stream flow upon nearly hori- 
 zontal beds of the ordinary brick-red Permian sandstone, which towards 
 its base, about Carronbridge, begins to contain small fragments of por- 
 phyrite, and to show, by the gradual increase of its volcanic detritus, 
 the approach of the underlying volcanic group of rocks. Some excellent 
 sections of this part of the sandstones have been laid open along the 
 sides of the high road to the north of Carronbridge. Thin lenticular 
 layers of gravelly volcanic detritus form there a marked feature among 
 the beds of sandstone. In proceeding up the Carron Water, we advance 
 on the whole into lower strata, though the angle of dip is always 
 low, and, owing to many slight undulations, the same beds are repeated. 
 A few small faults likewise occur, with the effect of occasionally 
 bringing up the underlying volcanic zone as well as the Carboniferous 
 sandstones to the surface. In the descending order of the Permian 
 strata, their volcanic history becomes more and more marked. The 
 tuffs increase in coarseness and in the tumultuous character of their 
 agglomeration, showing that the points of eruption must have lain in 
 this part of the basin. No actual volcanic neck or pipe, however, 
 was observed, unless we are to regard some of the masses of coarse 
 unarranged agglomerate as marking the site of orifices of eruption. 
 Nothing could be more characteristically volcanic than the coarse 
 brecciated agglomerates of the Carron Water, particularly near the 
 Wee Cleuch Bum, and about Jenny Hare's Bridge, where some of the 
 enclosed blocks must weigh half a ton or more. The tuffs and volcanic 
 sandstones contain some well marked beds of porphyrite, seen at and 
 above Durrisdeer Mill and Stanebutt. These are truly interbedded or 
 contemporaneous lavas, presenting sometimes a rather uneven surface, 
 upon and against which the coarse tuffs have been accumulated. At 
 several places (as at Enoch Waulk Mill and above East Morton) a 
 feature may be observed in the upper surface of some of the porphyrite 
 beds, which has been described as characteristic of certain Old Red 
 Sandstone porphyrites in Ayrshire — vertical veins of sandstone which 
 have arisen from the washing in of sand into cracks on the surface 
 of the cooled lava, before the deposition of the next succeeding 
 rocks. 
 
 68. Beyond the limits of the ThornhUl basin further evidence exists 
 of the former extension, not only of the Carboniferous but of the 
 Permian rocks, and especially of the volcanic portion of the latter 
 series. The largest and most interesting outlier occurs at Locherben 
 in the Garroch Valley abeady (par. 58) alluded to. The Carboniferous 
 strata occupy the northern half of this little basin. Their junction 
 with the Silurian rocks is obscured by the thick covering of alluvial 
 
35 
 
 gravel and peat. Where exposed, they consist of white, purplish, and 
 yellow gritty sandstones, lying nearly flat or with a gentle dip to the 
 south-east. In the course of the Garroch "Water, and about a quarter 
 of a mile to the west of Locherben, the junction of the Carboniferous 
 with the overlying Permian series is seen. The following is the 
 section : — 
 
 '_ . ( c. Purplish-grey amygdaloidal porphyrite. 
 
 i-ermiaii. | j_ rpj^j^^ ^^^ ^j ^^^ ^^^^ breccia. 
 
 Carboniferous. a. Eed and liver-coloured sandstone. 
 
 The thin bed of breccia, which here forms the basement of the 
 Permian rocks, consists of angular Silurian fragments intermingled 
 with blocks of vesicular and scoriaceous porphyrite, similar to the 
 sheet immediately overlying, and to those of the Thornhill basin, 
 imbedded in a brick-red ashy paste. The porphyrite is a close- 
 grained, finely crystalline, ferruginous rock, becoming towards the 
 base highly amygdaloidal, earthy, and scoriaceous. The southern half 
 of this basin is occupied by a coarse gravelly breccia, made up of 
 angular Silurian fragments and numerous porphyrite bombs. Here and 
 there thin seams and lenticular beds of soft red sandstone are met 
 with. 
 
 J. Briok-Eed Sandstones. 
 
 69. Owing to the rise of the volcanic zone into a ridge which crosses 
 the basin above Carronbridge, the Permian sandstones of the Thornhill 
 basin are thrown into two areas. That which lies to the north has 
 been described as lying along the course of the Carron Water, and 
 presenting a remarkable intercalation of volcanic materials. The 
 southern and much larger area contains on its northern margin mingled, 
 volcanic detritus in its lower beds. But over the central and southern 
 portions of the sheet, neither lava beds nor traces of tuff occur. The 
 volcanic action, therefore, which was so abundant and prolonged, must 
 have been extremely local; since, so far as observed, none of the showers 
 of volcanic dust fell over the southern parts of the basin. With the 
 absence of volcanic material, the normal character of the brick-red 
 Permian sandstones extends throughout the rest of the Thornhill area. 
 They are tolerably uniform in texture, colour, and in abundant false- 
 bedding. Though apt to darken from a cryptogamic crust which over- 
 spreads them, the sandstones continually expose fresh surfaces with 
 the remarkably bright orange or brick-red hue which distinguishes 
 them, and forms so singular a feature of the scenery in which they 
 take their part. Good sections have been cut in the gorge of the 
 Crichope ; the sandstones may also be seen to advantage in the quarries 
 at Gatelawbridge. 
 
 70. The Map shows on what uneven a floor the Permian series of 
 rocks was laid down. While in the northern portion of the basin the 
 succession of strata is most complete, towards the south the volcanic 
 zone disappears, and the brick-red sandstones, sweeping across the ends 
 of that zone as well as the Carboniferous rocks underneath, come to 
 lie directly upon the Lower Silurian hills. 
 
 71. The former wider extension of the brick-red Permian sandstones 
 was alluded to in par. 68. Besides the outlier there described, another 
 smaller patch of the same breccia is exposed on the western slope of 
 MoUins Hill, resting on the Silurian base of the district. 
 
36 
 
 II. — Dumfries Basin. 
 
 72. Only a portion of this basin comes within the present Map. It 
 contains no Carboniferous rocks, and the volcanic Permian zone is 
 wanting. Its long axis runs from north-west to south-east, or nearly- 
 parallel with the course of the Mth. The rocks consist of breccias and 
 overljdng brick-red sandstones. As a rule they dip away from the 
 Silurian strata which enclose the basin ; those to the east of the Mth 
 being inclined to the west and south-west, while those on the west side 
 dip to the east and north-east. The unconformity between these red 
 rocks and the underlying Silurian masses is well seen in one or two 
 places, as in the Cargen Water near the Glen Mill. In the northern 
 and eastern portions of the basin, the beds consist chiefly of brick-red 
 sandstones with marked false-bedding, exactly like those of the Thorn- 
 hill area; while the most of the ground to the west of the Nith is 
 occupied by a coarse breccia. This rock, which is extremely tough, 
 forms a well marked ridge extending from Terraughtie to Cargen. 
 The railway cutting near Groldielea affords an excellent section of this 
 breccia. It is made up of angular and subangular fragments of various 
 rocks embedded in a gritty paste. By far the commonest ingredients 
 are grey and purplish greywackes, with greywacke,- grey shale, and 
 pink felstone. Along with these have been noticed crystalline schistose 
 rocks and dark porphyrites. The following percentage was taken from 
 this section : — 
 
 Pink felstone with hornblende, 
 Grey and purplish greywacke, 
 Grey shale. 
 Quartz rock. 
 Grey schist, 
 
 34 per cent. 
 29 „ 
 28 „ 
 
 6 „ 
 
 3 „ 
 
 100 
 
 Along the western margin of the basin these breccias rest directly on 
 the Silurian rocks, but to the east of Dumfries they are interbedded 
 with the red sandstones. While carrying on the mining operations at 
 Mabie, some casts of fossUs were found in the strip of breccia near 
 Burnside west of Cargen. They were indeterminable owing to the 
 imperfect nature of the casts, but seemed to have been derived from 
 older palaeozoic rocks. 
 
 Miocene ?— I gneous Rocks. 
 
 73. Two instances have been found of basalt-dykes traversing the 
 Silurian rocks ; one on Trostan Hill four miles west of Moniaive, and 
 the other on Craigmuie Moor, half a mile south of Castlefem. The 
 rock is dark and compact, with crystals of plagioclase felspar. Kernels 
 of tachyUte were noticed near the edges of the Trostan dyke. The 
 date of these dykes cannot of course be determined from the evidence 
 obtainable in this district. It has been already shown {Explanation 
 to Sheet 14) that the abundant east and west or south-east and north- 
 west basalt-dykes which traverse the country, may with probability be 
 referred to the Miocene period. The Trostan dyke shows the charac- 
 teristic north-west direction. 
 
 Drift. 
 
 74. Within the limits of this Map there are clear proofs of the 
 extreme glaciation to which the country has been subjected. Following 
 
37 
 
 the order adopted in former Explanatims, the evidence will be here 
 arranged under the heads of (a.) Striated Eock Surfaces; (b.) Boulder 
 Clays; (c.) Sands and Gravels; (d.) Erratic Blocks; («.) Brick Clays; 
 , (/.) Moraines. 
 
 75. (a.) Striated Eock Surfaces.— The passage of ice over this 
 region is evident from the rounded outline bf the general surface of the 
 country. Not only the hills, but the smaller rocky knolls, still preserve 
 this uniformity of feature. Even where the rock surfaces have been 
 exposed for a time, their ice-worn character is apparent. In many 
 places good instances of roches moutonndes are to be met with ; and 
 the ice-markings, though irregular in their occurrence, are very numerous 
 in the valley of the Ken. Near Dairy, and on the left bank of Loch 
 Ken south of Balmaclellan and close to New Galloway Station, the 
 polished and striated surfaces are wonderfully fresh. The relation 
 between the striae occurring in this district and the form of the ground 
 is worthy of note. In the valleys of the Scar, Shinnel, and Dalwhat, 
 the direction of these marMngs is south-easterly, indicating that the 
 ice must have moved downwards from the high grounds round the 
 sources of these streams. And so also the same trend is to be found 
 in the upper reaches of the Ken, produced by the ice moving off from 
 the Cairnsmore region. But the striae found in other portions of the 
 Map prove very clearly that the high grounds to the west formed the 
 great central axis of dispersion for the ice which crossed Galloway. A 
 glance at the Map will show that the striae near the junction of the 
 Deugh with the Ken have an easterly trend, and though they swing 
 round to the south-east in the neighbourhood of Dairy and Loch 
 Ken, yet it is evident that a vast mass of ice must have continued its 
 easterly course. This is apparent from the markings found on the 
 top of the Keir Hills, which point nearly due east, as well as from 
 those on the moors south of Moniaive, and on the hilly ground 
 between Corsock and Dumfries, where their trend varies from 5° to 25° 
 south of east. The ice must have crossed the transverse valleys in 
 the southern portion of the sheet, overtopping the hills in its path 
 until it reached the Nith, where its course was deflected towards the 
 south. 
 
 76. (b.) Boulder Clays. — As in other districts in the south of 
 Scotland, the boulder clays of this region vary considerably in their 
 nature and mode of occurrence. The general character of these deposits 
 is that of a tough tenacious clay quite devoid of stratification, packed 
 with smoothed and scratched stones of different sizes. Occasionally the 
 polished boulders measure from 3 to 4 feet in diameter, but these are not 
 of frequent occurrence. In the north-western portions its colour varies 
 from a blue to grey and fawn colour, but towards the south it has a 
 brownish-red tinge, owing to many of the bands of the Queensberry 
 series having a similar tint. In the Thornhill and Dumfries basins the 
 colour is brick-red, from the presence of Permian sandstone. The 
 character of the stones embedded in the boulder clay corroborates the 
 evidence furnished by the striae as to the direction of the ice-flow. In 
 the Ken Valley north of Smeaton Bridge and its tributaries, numerous 
 blocks of Cairnsmore granite occur together with stones of more local 
 origin. One or two instances of granite from the same source have 
 been observed in the till sections in streams draining into the Castle- 
 fern Water and Black Mark Burn, but none have been noted south of 
 this point. In the lower portions of the Dalwhat, Shinnel, and Scar 
 Waters, boulders of Caradoc conglomerate likewise exist in the till. 
 No granite stones from the mass south-west of Loch Ken have been 
 
38 
 
 found in this deposit near Balmaclellan or in the district which stretches 
 from thence south-east to the Urr. Similar evidence is obtained from 
 the sections in the Thornhill and Dumfries basins, where greywackes, 
 felstones, and grits are mixed with Permian breccias and sandstones. 
 Though in general the character of the boulder clay is siich as has been 
 described, yet sections are to be found in the low grounds of a different 
 nature. Near Auchenaight, along the road leading from Penpont to 
 Maxwelltown, and again near Dunscore, sections are to be met with 
 consisting of a stony, earthy, and sometimes sandy matter, with sub- 
 angular stones, hardly any of them scratched, resembling the upper 
 boulder clay of other districts. 
 
 77. North of a line drawn from Balmaclellan by Corsock to the 
 Brooklands, thence north-eastwards by Larganlee Hill to the north edge 
 of the Dumfries basin, the boulder clays, with a few exceptions, are 
 spread over the surface of the country in the form of long undulating 
 slopes, and in the narrow valleys in the form of broad terraces thinning 
 out along the hillsides. In these terraces cuttings have been made by 
 stream action, varying in depth from 10 to 30 feet. This latter feature 
 is well developed in the upper reaches of the Ken, and in the Dalwhat 
 and Shinnel Waters and their tributaries. But south of the line already 
 indicated, the boulder clay occurs in the form of ' drums,' which are 
 seen to advantage in the moory tract south of Balmaclellan. There 
 they assume the shape of parallel ridges varying in length from 150 
 yards to a quarter of a mile. Sometimes the distance between these 
 ridges does not exceed 200 feet, though as a rule it is much more ; but 
 in every case the edge of the ' drum ' on either side is defined by a sharp 
 and well marked line. The intervening spaces are often covered with 
 peat or alluvium, probably representing silted-up tarns ; but usually it 
 is merely a rocky surface with a scraggy covering of herbage. These 
 rocky surfaces are well polished and preserve fresh striae. Often it 
 happens that a solitary ' drum ' has been left in the centre of a small 
 area which is almost bare of drift, though perhaps in the shallow 
 hollows between the rodhes moutonnies there may be a thin layer of 
 boulder clay too small to be expressed in the six-inch Map. Frequently 
 the 'drums' occur in groups, with the ridges joined to each other, but 
 in these instances the parallel arrangement is not so well marked. Their 
 height varies from 20 to 100 feet. From a general view of the disper- 
 sioji of these ' drums,' it seems evident that the well defined line round 
 each ridge is the result of original deposition and not of subsequent 
 denudation. Further, the long axis corresponds generally with the 
 direction of the strise on the adjacent roches moutmnies ; and lastly, 
 they seldom or never occur in the high grounds, but attain their greatest 
 development in the mossy and comparatively flat-lying districts. 
 
 78. Instances are to be met with in which beds of sand and gravel 
 are intercalated with the till. One example is to be found in the 
 Stroanfreggan Burn opposite the Knowe of Carroch, and another about 
 500 yards farther down the same stream on the left bank. In both 
 cases they are capped by a deposit of stiff boulder clay with scratched 
 stones. 
 
 79. Where a good section is obtained of the boulder clay to the east 
 of the Nith, it is usually seen to contain intercalated beds and numerous 
 ' nests ' of gravel and tough sandy clay. This character is well seen in 
 the stream that flows south-west past Garroch Cottage, in the Bran 
 Burn at the outcrop of the black shales, and also in the Chapel Burn 
 near Locherben. 
 
 80. (c.) Sands and Gravels. — This series is well represented in 
 
39 
 
 different portions of the Map. Covering nearly the whole of the 
 Dumfries basin, it stretches northwards along the narrow valley of the 
 Nith at Blackwood, circling round the White Spots and Kirkpatriok 
 Hills till it reaches Closeburn, where it again attains a great develop- 
 ment. Isolated but well marked kames occur on the Crichope Burn 
 near DoUard at a height of 600 feet. Instances are not wanting of the 
 gravels crossing different watersheds in this district. From Barjarg 
 the deposit sweeps across the ridge which divides the Mth from the 
 Cairn by Auchenage to Fardingjames, winding round the Fleuchlars 
 Hill. Again, it stretches along both sides of the valley of the Cairn 
 to Moniaive at an average height of from 400 to 500 feet. In both 
 valleys the gravel is heaped up in the form of ridges which often unite, 
 leaving a basin-shaped hollow in the centre filled with water, though 
 the lochan is frequently supplanted by alluvium or peat. These hollows 
 are seen to advantage in the neighbourhood of Dumfries, also south of 
 Auldgirth, and at Braco north of Dunscore. Good sections are exposed 
 in the various pits, showing the ridges to be made up of fine well- 
 water-worn gravel and sand ; the disposition of the stratification being 
 often coincident with the external form of the mound. Again, this 
 series may be traced along the banks of the Old Water, a tributary of 
 the Cairn, as far as Glenkiln and Cornlee, thence up the Glen Burn, 
 crossing the col to the Brooklands Burn, where it occurs near Larg- 
 hill at a height of 725 feet. Isolated gravel mounds are seen in the 
 Auchenhay and Knaril Burns, at a height of 700 feet, at Barnhillies, 
 and in other portions of the Map. A group of mounds occurs near 
 Manwhill at a height of- 925 feet, which probably belongs to this 
 series. There are few obtainable sections, but this conclusion seems 
 natural from the well-rounded character of the stones as well as from 
 the distinct stratification. Towards the upper limits of the gravel in 
 the main valleys, a deposit is met with which differs in a marked 
 degree from the ordinary character of the gravel series. It consists 
 of a stony, sandy, and clayey matter, with numerous angular, sub- 
 angular, and rounded stones — the stones and matrix being frequently 
 firmly welded together. Pits have been dug in this stuff near Brecon- 
 side Tower, and near Woodhead and Glengaber in the neighbourhood 
 of Dunscore. This may, perhaps, indicate the relics of the moraine 
 matter from the denudation of which the sand and gravel series was 
 largely derived. 
 
 81. (d.) Erratics. — Boulders of Caimsmore granite are scattered 
 over the hills to the south-east, as, for instance, on the Stroanpatrick, 
 Culmark, Fingland, and Lochlee Hills ; and one has been noted on the 
 west face of the Nether Hill at a height of 1000 feet, eight miles distant 
 from its source. Boulders of Caradoc conglomerate are distributed 
 over the ridges dividing the Dalwhat, Shinnel, and Scar Waters, and 
 the hilly ground north of Penpont ; while, again, blocks of greywacke 
 have been found within the granite area south-west of Loch Ken. A 
 noticeable feature connected with the distribution of these erratics 
 is the non-occurrence of Mabie granite boulders in the ground to the 
 north, and the absence of Dee granite boulders from the ground to the 
 east of Loch Ken. Both the positive and negative evidence in this 
 sheet seems to indicate that the erratics lie chiefly in the line of the 
 old glaciers ; and though it cannot be doubted that boulders were 
 scattered far and wide during the great submergence from their 
 presence on the tops of kames, yet it would appear that many of 
 them must have been distributed during the great extension of the 
 ice. 
 
40 
 
 82. («.) Brick Clays. — The representatives of this series occur on 
 the right and left banks of the Mth at Dumfries. Excellent sections 
 are exposed in the pits at the brick works, where thick deposits of fine 
 clay are overlaid by gravel and sand forming part of the raised beach. 
 The following section is taken from the pit at the Ryedale Brick 
 Works : — 
 
 1. Gravelly earth atop. 
 
 2. Layers of fine gravel, 2 to 3 feet. 
 
 3. Thick bed of fine sand, 8 to 10 feet. 
 
 4. Thick deposit of fine clay, upwards of 14 feet, htit the bottom of this clay is 
 
 not seen. It contains hardly any stones. 
 
 The thickness of alluvial matter overlying the clay in this section 
 does not differ much from that seen in the Hannahfield Pit on the left 
 bank of the river. The latter section exposes the following beds : — 
 
 1. Surface soil, 1 foot. 
 
 2. Fine gravel, 2 feet. 
 
 3. False-bedded sand passing down into fine loam, 2 feet. 
 
 4. Alternating beds of fine gravel and sand, 2 feet. 
 
 5. Thick bed of clay free from stones, upwards of 10 feet — bottom not reached. 
 
 It is evident that these fine clays belong to the glacial series, 
 though shells are not abundant. Shells are said to have been got 
 from the brick field near Cargenholm which has lately been covered 
 over. From the Ryedale and Marchhill Pits two or three species of 
 Foraminifera and one of Entomostraca have been obtained. 
 
 83. (/.) Moraines. — It is impossible within the limits of this 
 Explanation to give a detailed account of the various groups of 
 moraines occurring in this Map, or to enter into the question of their 
 relation to the other members of the drift series. The most important 
 groups of moraines form part of a continuous series which stretches' 
 westwards into the high grounds in Sheet 8, and a full discussion of 
 them is reserved for the Explanation of that Sheet. It will be sufiicient 
 for the present if the various localities where they occur are indicated 
 along with some of their chief features. 
 
 The mass of high ground round Cairnsmore of Carsphairn nourished 
 an independent series of glaciers towards the close of the glacial 
 period, which have left their traces in all the valleys draining the 
 eiistern side of the range. In the Benloch Burn, which springs from 
 the south slope of Cairnsmore, good sections of moraine matter are 
 exposed, which is spread irregularly along the hillsides. Similar 
 sections are to be found in the Clennoch Burn, draining to the north. 
 But by far the best marked group connected with this chain, is that 
 which occurs in the Poldover Burn. The broad peaty col east of the 
 Gairy of Cairnsmore is strewn with moraine heaps, which may be traced 
 along both sides of the stream just mentioned to Moorbrock. The 
 mounds are not continuous as far as this point, but are to be found at 
 intervals, increasing in size at the Eider's Knowes and at Moorbrock, 
 where they vary in height from 10 to 30 feet. Near the col, where the 
 two main burns unite, there is a little alluvial patch behind a series of 
 moraine heaps, probably marking the site of an old- lochan. Good 
 sections are exposed both in the streams and at Moorbrock, showing 
 the stuff to consist of loose gravelly rubbish with tolerably well rounded 
 but rarely scratched stones ; while on the tops and sides of the mounds 
 are perched boulders of granite and metamorphosed greywacke. On 
 the south-eastern face of Knockwhirn, -a ridge strewn with greywacke 
 boulders is traceable along the slope, which is undoubtedly a lateral 
 
41 
 
 moraine. Again, behind the Nether Holm of Dalquhairn, and along 
 the eastern side of the Do(Jd Hill, there is a detached group of mounds 
 at a height of from 1000 to 1200 feet. These are in all likelihood 
 traces of the glaciers which filled the valleys to the north (see Exjplan, 
 Sheet 15, pars. 100, 101). 
 
 84. By far the largest and most important series of moraines met with 
 in this part of the sheet occurs in the valley of the Deugh. This valley, 
 only a small portion of which is seen in the Map, formed the great 
 outlet for the later glaciers which moved off from the high grounds at 
 the north limit of the Kells range. From the size of the moraines, as 
 well as from the extent of country over which they are spread, it is 
 evident that the later glaciers, though small in comparison with the 
 great extension of the ice, must have attained considerable dimensions. 
 From the margin of the Map, the moraines are traceable eastwards by 
 Marscalloch and Muirdrockwood, where they cross the Ken to Stroan- 
 freggan and the Carroch Lane, circling round the Blackmark Hill 
 towards the county boundary. In the Deugh the mounds are arranged 
 in concentric lines, sometimes conical in shape, but generally assuming 
 the form of narrow ridges which often trend towards the centre of 
 the valley. The successive ridges are admirably seen while walking 
 along the Deugh Eoad to Carsphairn, where their truncated ends are 
 exposed in cuttings, and where patches of peat may be seen filling up 
 the intervening spaces. In most of these sections the moraine matter 
 consists of a sandy clay with numerous subangular stones, which in 
 many instances have irregular striations. Towards the base of the 
 cuttings the stuff is much more compact, and as a rule there is no trace 
 of stratification in this deposit. The embedded stones vary in character 
 but consist mostly of grits, greywackes, felstones, black shales, and 
 conglomerates, which occur in situ to the west ; while boulders of a 
 somewhat similar nature rest on the tops of the mounds. It is 
 important to note that in the Ken between Muirdrockwood and Bridge- 
 mark, a thick deposit of tough boulder clay underlies the moraine 
 heaps, excellent sections of which are exposed along the river-course 
 from Smeaton to the high bridge of Ken. 
 
 85. Moraines occur in some of the tributaries of the Ken on the 
 west side, but a description of them falls naturally into the Explanation 
 of Sheet 8. Along the valley of the Ken from the Deugh to New 
 Galloway, there is but a sparse covering of drift. Continuous with the 
 Deugh series of moraines, a deposit is traceable southwards on both 
 sides of the river, which appears often in the form of mounds. From 
 the general character of the sections there can be little doubt that it 
 is allied to moraine matter, though it is highly probable that the 
 materials were subjected to some rearrangement during the act of 
 deposition. Near Glenhowe, Strangassel, MUlquarter, and at other 
 localities, pits have been dug in this stuff. It consists of a sandy and 
 stony matter with tolerably well rounded stones, which are often large 
 and subangular. Generally the sections exhibit stratification, some- 
 times rude, but frequently of a distinct type. From the resemblance 
 between these sections and others in the sheet to the west, it is highly 
 probable that this is a species of moraine matter. (Par. 80.) 
 
 86. Another important group of moraines occurs in the Dee, in the 
 heart of the mass of granite. From the Crannoch Ford they extend 
 southwards to the Nether Orchars, where they attain a considerable 
 size, varying from 20 to 30 feet in height, and thickly strewn with 
 granite boulders. East of the Shaw Hill towards the Dee, the ground 
 has a hummocky contour, but covered for the most part with peat and 
 
42 
 
 revealing no sections. In all likelihood the hummocks are half-con- 
 cealed moraines, a supposition which is strengthened by the fact that 
 the Glengainoch Burn contains a well marked series. 
 
 87. The only group which remains to be noticed occurs in the 
 neighbourhood of Loch Urr. This series claims special attention from 
 the fact of its being completely isolated from any great mass of high 
 ground. The ground over which it is spread, is more than twelve miles 
 distant from the great Kells range. The size of the mounds, the large 
 Bubangular boulders perched on their tops, as well as their distance 
 from any suitable gathering ground for glaciers, indicate that these 
 moraines date in all probability from the great extension of the glaciers. 
 They extend from Loch Urr eastwards by Craigenvey to Sundaywell Moor, 
 then south-westwards along the valley of Castramont to Craigenputtock. 
 These mounds are best seen in the valley east of Loch Urr near Craig- 
 envey, where they cover the bottom of the valley and extend for some 
 distance up the hill-slopes. They cross the watershed and reach a still 
 greater development on the east side of the col. At this point they 
 are covered with large angular greywacke blocks. In shape they are 
 irregular and hummocky, sometimes running across the valley. Good 
 sections of the stuff are met with on the roadside leading to Loch Urr. 
 It consists of a gravelly unstratified earth, the stones being in some 
 parts quite angular and in others well rounded. Where the angular 
 stones occur in a stiflfer part of the earth, the deposit resembles moraine 
 matter ; but where they show a rounded appearance, it looks more like 
 coarse earthy gravel. The mounds tail off near the junction of the 
 Shillingland with the Castramont Burn, at a height of about 400 feet 
 above the sea. 
 
 88. Lochs. — The sheets of water occurring within the boundaries of 
 the Map, are mainly connected with the glacial period. Of these lochs, 
 about 30 in number, by far the largest is Loch Ken. Situated in the south- 
 west corner, it stretches from the Holms of Kenmure to the edge of the 
 sheet, a distance of four miles. At its northern limit where it receives 
 the waters of the Ken, it is being slowly silted up ; while towards 
 the south it unites with the Dee. For nearly two miles it is flanked on 
 the west by the slopes of the Bennan Hill, which rise abruptly from the 
 water-lip. Its breadth near Lochside is about 700 yards. Ice-worn sur- 
 faces of rock occur along both banks, while roches moidormies peer above 
 the water in the centre of the loch. Many of these polished surfaces 
 stUl preserve the striae, the direction of which coincides in the main with 
 the long axis of the loch. In this neighbourhood there are abundant 
 proofs of the extreme glaciation to which the ground has been sub- 
 jected ; and, viewing this in connection with the evidence furnished by 
 the loch itself, there can be little doubt that this shallow hollow has 
 been eroded by the ice. With one or two minor exceptions, the rest 
 of these sheets of water owe their existence to the irregular deposition 
 of the drift. Some of these lie in hollows in the boulder clay or 
 moraine debris — as, for instance. Lochs Urr, Eegland, Marstintown, 
 Areeming, and Patrick ; others, again, rest partly on drift and partly on 
 rock. The latter are the most numerous, comprising nearly all the 
 main lochs ; Lochinvar, Corsock, Auchinreoch, and Lochrutton Lochs 
 being good cases in point. The group which occurs on the north-west 
 face of the Black Craig Eidge, viz., Lochs Howie, Skae, Brack, and 
 Barscobe, are worthy of note, as they have certain features in common. 
 Nearly in one line, and not far from the same level, they are encircled 
 by ridges of boulder clay on the north ; while to the south there is the 
 rocky slope, bare of drift. They have found outlets by cutting small 
 
43 
 
 channels through the drift, and as these are being deepened by con- 
 tinual erosion, the lochs must eventually dry up and be replaced by 
 alluvial patches. In a similar manner many of the peaty and alluvial 
 flats have originated, which are now met with in various portions of the 
 Map. They evidently mark the sites of former lakes, which have been 
 drained by stream action ; but in those cases, where isolated lochans 
 with no outlet lay in hollows between the gravel kames or moraine 
 mounds, they have been supplanted by peat. (Par 91). 
 
 ^Raised Beaches. 
 
 89. Extending along the face of the abrupt and craggy hill which 
 rises behind Locherben and looks south-west, three distinct ledges or 
 narrow terraces are seen rising one immediately behind the other, the 
 remarkable horizontality of which presents a conspicuous appearance 
 from the road. The highest of the three lies at a height of about 1100 
 feet above the sea. The second or central terrace coincides with the 
 1000 feet contour line. The lowest, which is exceedingly well marked, 
 stands at a height of 980 feet, and extends from Garroch to the Capel 
 Burn, where its continuity is broken, a distance of more than a mile. 
 A prominent cliff of this terrace overhangs the opposite bank of the 
 stream, and fringes both sides of the col leading to the Bran Burn. 
 These platforms are to some extent cut out of the solid rock and form 
 indentations in the hillside, but for the most part they are projections 
 of gravel. The Capel Burn exposes a good section of the lowest 
 terrace, where it is seen to consist of coarse but well water-worn gravel 
 intermingled with sand, overlying a considerable thickness of fine sand 
 with false and contorted bedding, and which in turn rests on stiff red 
 boulder clay. There seems to be an entire absence of fossils. 
 
 90. In the south-west corner of the sheet, on the right bank of 
 the Nith, a strip of flat low-lying land extends from Troqueer Holm 
 to Kirkconnell Moss. This strip indicates the existence of former 
 sea-levels. The oldest of these terraces extends from Park, near 
 Maxwelltown, southwards to Cargenholm, at an average height of 
 about 50 feet. Excellent sections of this terrace are seen at the 
 Eyedale Brick Works, where it consists of well water-worn gravel 
 and sand arranged in distinct layers, with marked false bedding. 
 This old sea-beach has been much cut up by recent denudation, but 
 there are still marked traces of its existence. No organic remains 
 have yet been found in these sands and gravels, which cap the glacial 
 clays. The flats of Cargen represent the more recent terrace, which 
 shades gradually upward into the 50-feet beach. The average height 
 of this terrace is about 25 feet. It is traceable almost continuously 
 from this point to the mouth of the Nith, where it forms a broad 
 margin of richly-cultivated land. 
 
 Peat and Alluvium. 
 
 91. The alluvial deposits have been formed chiefly by the action of 
 streams and rivers, and naturally occur along the main hues of drainage. 
 Some of the main patches are to be met with in the course of the Nith, 
 stretching from Dumfries northwards to Auldgirth, and again from 
 Bamdennoch by Thomhill to Carronbridge. Other patches occur along 
 the banks of the Cluden and the Cairn below Moniaive, while still 
 another rich alluvial flat is traceable along the Ken from New Galloway 
 
44 
 
 northwards to Dairy. In several instances a series of terraces is met 
 with in the larger river-valleys, which indicate previous stream-levels — 
 the highest, of course, being the oldest. In the neighbourhood of 
 ThornhUl there are three well marked terraces distinctly recognisable 
 in different parts of the basin. There are other patches of alluvium 
 in the Map, more limited in extent, which have a different origin. They 
 lie in many cases iu hollows in the drift, and doubtless represent old 
 lakes which are now silted up. Several good instances are to be found 
 in the Dumfries basin, in the midst of the sand and gravel series. As 
 has already been explained, several of the lochs in this sheet owe their 
 existence to barriers of boulder clay, which are being slowly cut through 
 by the streamlets draining the lochs. The deepening of the channel 
 gradually decreases the size of the loch, so that the former limits of the 
 sheet of water are indicated by an alluvial or peaty flat. This process, 
 coupled with the silting-up of lakes, may explain the existence of these 
 outlying patches. 
 
 92. The rough moorland districts in the central portions of the Map 
 are covered with heather and patches of thin peat. Here and there in 
 hollows, the peat thickens and forms mosses of considerable extent. 
 The most important of these are indicated on the Map. They occur 
 chiefly in the basin of the Urr, and they are likewise scattered over 
 the moory ground which stretches westwards towards the Ken. Many 
 of these peat deposits fill up hollows between the ' drums,' but as a rule 
 they rest irregularly on rock and drift. By far the largest mass of 
 peat in the Map stretches from Dalskairth to Kirkconnell (Sheet 10), 
 a distance of about three miles, with an average breadth of half a mile. 
 This area has been reclaimed to a large extent, as, for instance, between 
 Laneside and Mabie Lodge ; in the neighbourhood of Kirkconnell the 
 peat is of considerable thickness and of excellent quality. An attempt 
 has recently been made to utilize the peat in Kirkconnell Moss, which 
 was for a time successful, but owing to the rapid fall in the price of 
 coal, the project has been abandoned. 
 
 93. An important discovery was made near Cargen, which is worthy 
 of note, as indicating previous oscillations of the sea-level, as well as 
 probably affording traces of neolithic man.^ During the sinking of a 
 well through the raised beach at Islesteps, close to the Cargen Water, 
 the following section was passed through, — sand, silt, etc., 15 feetj 
 peat, 18 inches; stiff clay, 14 feet; while, underneath the clay, gravel 
 was pierced. In this peaty layer the remains of a fir-tree were 
 found with its roots penetrating the underlying clay, and close by 
 were discovered many bits of charred wood, bundles of moss, and 
 traces of phosphate of iron. The thick mass of clay underneath 
 the peat is doubtless the same deposit as that which is now worked 
 at Eyedale and Hannahfield, and which was formerly worked about 
 half a mile up-stream from Islesteps. It seems to occupy a similar 
 position. The layer of peat is not seen, however, in the pits at 
 Dumfries. In this section the clay (in which marine shells have 
 been found) evidently proves the presence of the sea ; while the layer 
 of peat, with the remains of trees and charred wood, points to the 
 upheaval of the searbed, the subsequent growth of terrestrial vegetation, 
 and (unless the presence of the charred wood can be accounted for by 
 lightning or other natural cause) the presence of man. The stratified 
 deposits above the peat indicate the submergence of the old land surface, 
 and the return of marine conditions. 
 
 ' This discovery was made by P. Dudgeon, Esq. of Cargen, wh.o_has supplied the 
 above information. 
 
45 
 
 94. Between Cargen and Mabie a canoe was dug out of the moss 
 many years ago. This canoe, which is still to be seen at Mabie, is 
 about 20 feet in length, and has been hollowed out of an oak tree A 
 bronze pot, said to be of Roman age, was also found in the same moss 
 near Kirkconnel. 
 
 Economic Minerals. 
 
 95 Building Materials.— The rocks comprised within the Map 
 furnish several varieties of building stones. In the Silurian areas the 
 massive Queensberry grits are extensively used for building purposes, 
 on account of their durability and regular system of jointing. Xhe 
 irregularly jointed greywacke bands in the Ardwell, Dalveen, and 
 Lowther Groups are not suitable for building purposes, though often 
 quarried for dry-stone dykes. The dark-blue flaggy shales of the 
 Lowther series at Benbuie in the Dalwhat Valley, and the blue shales at 
 Barlae and Marnhoul, which lie near the top of the Queensberry series, 
 have both been used for roofing purposes. They are not genuine slates, 
 however, as they have no cleavage planes, and on account of their 
 weight are not well adapted for the purpose. The granite of the 
 Loch Ken mass has recently been made use of for house building, 
 but only to a limited extent. The grey Calciferous Sandstones of the 
 Thornhill basin furnish excellent building material. They have been 
 largely quarried south of Drumlanrig and near Carronbridge, and in 
 the case of one or two recent local buildings) they have been preferred 
 to the well-known Gatelawbridge stone. But by far the finest building 
 stones are obtained from the Permian sandstones of Dumfries and 
 ThornhUl. The red sandstones vary considerably in quality, but at 
 Gatelawbridge and Locharbriggs they have long been worked. Owing 
 to their capabilities of being easily dressed, they are much less expensive 
 than some of the other building materials already referred to. While 
 much of the stone is extremely porous, many of the bands are very 
 durable, and are largely used for monumental purposes. Several of 
 the felstone dykes which traverse the Silurian rocks are quarried for 
 dry-stone dykes. 
 
 96. Limestones. — The only bands of limestone in this sheet are to 
 be met with in the Calciferous Sandstone series of the Thornhill basin. 
 One band has been worked at Barjarg, while others have been quarried 
 on the east side of the basin near Closeburn. The limestone is largely 
 used for agricidtural purposes in the surrounding districts. 
 
 97. EoAD Metal. — ^Among the Silurian rocks, the hard bands of the 
 Queensberry series are used for road metal where they can be con- 
 veniently obtained. The other members of the Llandeilo rocks are 
 sometimes quarried, but, owing to the shattery and jointed character 
 of the material, they are not so serviceable. Some of the supersilicated 
 felstones are used for this purpose, but are not so accessible as the 
 Queensberry grits. 
 
 98. Brick-Clays. — AtEyedale and Hannahfield near Dumfries, and 
 other places on both sides of the Nith, certain blue clays have been 
 used for the manufacture of bricks. These blue clays mostly underlie 
 the stratified sands and gravels of the 50-feet beach. 
 
 99. Ores. — Several thin veins of hematite occur in the SUurian 
 areas. In the neighbourhood of Mabie, among the metamorphic rocks 
 round the edge of the granite, an active search has recently been made 
 for workable veins of hematite, but the efforts have proved fruitless. 
 Another thin vein of hematite, indicated on the Map, is to be seen in 
 the Glenjaan Burn above Moniaive. 
 
46 
 
 100. Fuel. — Peat is the only kind of fuel to begot within the limits 
 of the sheet. The various mosses indicated on the Map, and specially 
 the Kirkconnell Moss, are largely used for this purpose. Several foolish 
 attempts have been made in search of coal among the black shale 
 bands in the Silurian areas. 
 
 Soils. 
 
 101. The nature of the soils is determined chiefly by the character 
 of the different geological formations occurring in the sheet. The 
 richest soils are to be found in the alluvial flats along the banks of the 
 main watercourses. In the Dumfries and Thornhill basins, and in the 
 valleys of the Cluden and the Cairn, where there is a wide distribution 
 of gravelly drift, the soils are generally light. The broad belt of undu- 
 lating ground which stretches from the Terregles Hills westwards by 
 Crocketford and Corsock, to Loch Ken, is covered ii-regularly with ' drums' 
 of boulder clay, which have been mostly brought under cultivation. 
 The SOU is generally stifi' and retentive. The same peculiarity is 
 characteristic of the valley of the Ken northwards as far as Glenhowl. 
 In the central and north-western portions of the Map, as well as the 
 high ground lying to the east of the Nith, there is a tolerably wide- 
 spread covering of boulder clay, as already described. Though much 
 of the ground in the lower parts of the valleys might be cultivated, as 
 in many cases it has been, it is now mostly used for pastoral purposes. 
 The smooth hill -tops and rock-slopes have a grassy or heathery covering, 
 but the soil is generally cold and stiff. 
 
APPENDIX. 
 
 I.— LIST OF LOCALITIES 
 
 FROM WHICH FOSSILS HAVE BEEN COLLECTED BT THE GEOLOGICAL SURVEY 
 IN WESTERN DUMFRIESSHIRE AND EASTERN KIRKCUDBRIGHTSHIRE. 
 
 (Sheet 9.) 
 
 The numbers are those by which the Localities are denoted in the succeeding 
 
 Lists. 
 
 Upper Llandeilo. 
 
 1. Glenessland Bum, above Sundaywell, about 4 miles W. of Dunsoore. 
 
 2. Craigdasher HiU, Glenessland Burn, Streamlet descending from, about 4J miles 
 
 W. by S. of do. 
 
 3. Craigdaaber Hill, at Wood, a little farther up Streamlet. 
 
 4. ,, about middle of "Wood. 
 
 6. ,, above "Wood, at division of Streamlet. 
 
 6. Glenessland Burn, below Castramon, about 5 miles "W. by S. of do. 
 
 7. Bogrie Burn, about balfway up, at junction with small Bum, 3J miles "W. of do. 
 
 8. Scar, i mUe S. by E. of Upper "Whiteside, 3 J miles "W. by S. of do. 
 
 9. Urr "Water, i mile S."W. of Nether Glaisters, about 7i miles S."W. of do. 
 16. „ i mile E. of Chapel. 
 
 11. „ in Field, 100 yards from Eiver. 
 
 12. „ 250 yards from Crogo Tower. 
 
 13. Glen, Bum S."W. of, about 5§ miles S."W. of Dunscore. 
 
 14. Old "Water, Tributary of, i mile "W. of Skeoch, 4 miles S. of do. 
 
 15. Auchenvey,Hill 350 yards E. of, about 5i miles E. by S. of Balmaolellan. 
 
 16. Urr "Water, opposite Knooklearn, TJ miles S.'W. of Dunscore. 
 
 17. Barend Burn, a few yards above road leading from Barend to Little Merkland, 
 
 about 4 J miles S. E. of Balmaolellan. 
 
 18. Barlae Quarry, 3 mUes N. of St. John's Town of Dairy. 
 
 19. Barskeoch Burn, 2 miles N. by "W. of do. 
 
 20. Arndarrooh, Streamlet a little S. of, 5 miles H". of do. 
 
 21. "Water of Ken, a little below Bridge, about 5i miles N. of do. 
 
 22. Deugh "Water, below Carminnow, about 6 miles N. by W. of do. 
 
 23. Stroanpatriok, Streamlet a little N. by E. of, about 7| miles N. of do. 
 
 24. Shinnel "Water, near Shinnel Head, 6 miles N.W. of Moniaive. 
 
 25. Dibbin Lane, half-way up Bum, about 6^ miles N."W. of do. 
 
 26. „ near source, about BJ miles N"."W. of do. 
 
 27. Manwhill, Streamlet i mile S.S."W. of, about 7i miles ■W.l!]"."W. of Moniaive. 
 
 28. Benbraok HOI, Streamlet at, 7J mUes ]Sr."W. of do. 
 
 29. Appin Bum, near head, about 6 miles N.N."W. of do. 
 
 30. Auchenhessnane Quarry, Scar "Water, about 4 miles N. by E. of do. 
 
 31. Clodderoch Bum, a little below old road leading from Moniaive. 
 
 Caradoc. 
 
 32. March Burn, hUlside near, 6 miles N. by "W. of Moniaive. 
 
 Carboniferous. 
 
 33. Limestone Quarries, 1 mile S.E. of Closebum. 
 33.* Crichope, above Closebum Mill, near Closebum. 
 
 Post Tertiary. 
 
 34. Ryedale Brick "Works, Maxwelltown. 
 36. MarchhiU Brick "Works, near Dumfries. 
 
48 
 
 II.— LIST OF FOSSILS. 
 
 In the following List of Organic Remains, the formations and beds are 
 arranged in ascending order. 
 
 Moffat or Hartfell Black Shale Group. 
 
 Name.' 
 
 ■His. . 
 
 Class, etc. 
 Hydrozoa (Oraptolitidce), — 
 
 Climaoograptus teretiusoulus. 
 
 Sp 
 
 Dicellqgraptus Forohammeri 1—Geinifz. . 
 Dicranograptus ramosus ? — Jlall. . 
 Diplograptus acuminatus ? — Nicholson. . 
 
 ,, cometa. — Geinitz. 
 
 ,, folium. — His. i 
 
 ,, palmeua. — Bare. 
 
 „ pristis. — His. . 
 
 „ tamariscus. — Nwholsan. . 
 
 „ Sp. (with distal vesicle) . 
 
 GraptoUtBus lobiferas. — M'Ooy. . 
 „ „ var Mooli, 
 
 ,, Nilssoni. — Barr. 
 
 „ Sagittarius. — His. 
 
 „ Sedgwickii. — Portlock. 
 
 „ „ var triangulatus.- 
 
 Eastrites peregrinus. — Barr. 
 
 „ Sp 
 
 Young Graptolites, .... 
 Dawsonia companulata. — Nicholson.^ 
 Crustacea (PhyUopoda), — 
 
 Discinocaris Browniana. — H. Woodward. 
 Peltocharis aptychoides. — Salter. . 
 
 Queensberry Grit Group. 
 
 Fucoids ? , . Chondrites regularis ? — Harkness. . 
 
 Triclioides ambitus ? — Harkness. 
 
 Palseochorda major ? — M'Goy. 
 Hydrozoa, . . Eemains of a Diplograptus, . 
 
 Protovirgularia dichotoma. — M'Ooy. ^ 
 Crustacea, . . Phacops ? Maaconochii, — Sp. nov.^ 
 Mollusca (Cephalopoda), — 
 
 Eemains of Ortlioceratites, . 
 
 Locality Number. 
 1,2,3,4,5,6? 
 7, 8, 9, 12, li, 
 16, 17. 
 10, 15? 
 1. 
 16. 
 9. 
 
 4, 8, 11. 
 4. 
 
 4, 5. 
 
 1,3? 6, 9,12? 
 14, 19. 
 49, 11, 12. 
 15. 
 4. 
 4,8. 
 
 4, 14. 
 
 2 ? 4, 5, 9, 11, 
 
 14. 
 
 2, 3, 4. 
 
 4,11. 
 4,11. 
 8. 
 3,7. 
 
 5, 6, 19. 
 
 11. 
 4. 
 
 18.' 
 18. 
 18. 
 18. 
 
 31. 
 
 30, 31. 
 
 ^ The genus Dawsonia was provisionally established by Professor Nicholson 
 (Annals Nat. Hist., 1873, xi., p. 139) for certain small rounded and compressed 
 bodies, common in graptolitic shales, and which he had previously on various occa- 
 sions described as ' grapto-gonophores ' (Geol. Mag., iii., p. 448), and 'ovarian cap- 
 sules' (Mon. Brit. Grap., pt. 1, p. 71, f. 41). 
 
 ^ From Locality 18 Professor Harkness obtained the following fossils (Quart Jour 
 Oeol. Soc, xi., pp. 473-476) :— 
 
 Fiu:oids, 
 
 Zoophytes, 
 Annelides, 
 
 Chondrites informis. — M'Ooy. 
 
 „ regularis. — Harkness. 
 Palceochorda major. — M'Ocry. 
 
 ,, ? teres. — Harkness. 
 Trichoides ambiguus. — Harkness. 
 Protovirgularia dichotoma. — M'Ooy. 
 Crossopodia Scotica. — M'Ooy. 
 Nerietes multiforis. — Harkness. 
 
 ^ Placed under the Hydrozoa provisionally only. 
 
 See p. 51. 
 
49 
 
 Class, etc, 
 Mucoids, . 
 
 Lowther Group. 
 
 Name, 
 
 . Palceochorda 1 — Sp. 
 
 Lead Hills Black Shale Group. 
 
 Hydremia (Corynoidea), — 
 
 Corynoides. — 8p.^ 
 „ {GraptoUtidcB), — ■ 
 
 Climaoograptus Hcornia, — Sail. . 
 „ teretiusoulus, — His. 
 
 Sp. . . . 
 DiceUograptus (Sp. a. and 6. ) 
 
 Sp. (c, M. 3950) . 
 Dicranograptus ramosus ? — Hall. . 
 
 Sp. (M. 3951) 
 Diplograptus Harknessi ? — Nicholson. 
 , , penna ? — Hopkinson. 
 
 ,, pristis, — His. . 
 
 Pleurograptus linearis. — Carruthers. 
 
 Sp. . . . 
 
 Dawsonia campaaulata, — Nicholson. 
 Brachiopoda, . . Acrotreta? Nicholsoni? — Davidson. 
 
 Locality Number, 
 
 26. 
 
 . . 24, 
 
 25. 
 
 
 
 . 24, 
 
 25, 
 
 26, 
 
 29. 
 
 , 20. 
 
 
 
 
 26. 
 
 
 
 
 27, 
 
 
 
 
 . 21, 
 
 24. 
 
 
 
 27. 
 
 
 
 
 . 26, 
 
 27, 
 
 29 
 
 
 . 26. 
 
 
 
 
 20, 
 
 21, 
 
 22, 
 
 24, 
 
 • 26, 
 
 26, 
 
 27 
 
 
 . 26. 
 
 
 
 
 . 28. 
 
 
 
 
 (21, 
 
 24, 
 
 25, 
 
 26, 
 
 ■ • i 27, 
 
 29. 
 
 
 
 25. 
 
 
 
 
 Caradoc (Fine Conglomerate). 
 
 Remains of Encrinite Stems, probably Glyptocrinus, .> 
 Orthis calligramma, J 
 
 Black Shale (fragments) in Conglomerate. 
 
 Two Small GraptoHtes, one probably a Diplograptus, 
 the other Climacograptus, .... 
 
 Carboniferous. 
 
 Closeburn Limestone. 
 
 Actinozoa, 
 JSchinodermata, 
 Brachiopoda, . 
 Gasteropoda, . 
 
 Cephahpoda, 
 
 Brachiopoda, 
 
 32. 
 
 32, 
 
 Zaphreutis cyHndrica. — Scouler. • 
 Stem of orinoid, . 
 Produotns giganteus. — Martin. 
 Bellerophon Sp. — (cast). 
 Euompnalus. — /Sp. (large oast. ) 
 Natica, ...... 
 
 Fragment of Orthooeras, 
 
 Shale in connection with Limestone. 
 
 Productus giganteus. — Martin. 
 
 ,, semireticulatus. — Martin. 
 
 „ „ var Martini. — Sow. 
 
 Spirifera. — Sp. (bad cast.) . . . . 
 Streptorhynchus crenistria. — Phil. 
 Edmondia or Sanguinolites, . 
 Schizodus. — /Sp. (small crushed casts.) . 
 
 33. 
 
 f/amellihranchiata, 
 
 Shale and Sandstone in connection with Limestone. 
 
 Pkmim, . 
 
 Polyzoa, . 
 Laimellibra/nchiata, . 
 
 Cephalopoda, . 
 
 Sphenopteris. — Sp. 
 
 Stigmaria, and other plant remains, 
 
 Fenestella. — Sp 
 
 Edmondia ? — Sp. (crushed cast. ) . 
 Schizodus. — Sp. (small crushed casts.) 
 Fragment of a Nautilus, 
 ' See p. 50. 
 
 33, 
 
50 
 
 Purple Shale, etc., on Cricliope Water, above Closeburn Mill. 
 
 Class, etc. Name. Locality Number. 
 
 Asterophyllites. — Sp. (remains of) 
 Calamites (large 8p. ) . . . . 
 Cyclopteris orbicularis. — Brong. . 
 Neuropteris LosMl. — Brong. 
 SphenophyUum. — 8p. (remains of) 
 
 Post Tertiary. 
 
 Brick Clays. 
 
 Foraminifera,^ . Polymorpliina fusiformis.^ — Roemer. . .34. 
 
 Polystomella striatopunotata. — F. & M. . 34, 35. 
 
 Nonioniua asterizans. — F. & M. . 34.. 
 
 Mitomostraca, . Specimen (unnamed). 
 
 III.— NOTES ON THE FOREGOING LIST. 
 Lower Silurian. 
 
 UPPER LLANDEILO. 
 Htdeozoa. 
 
 Genus Corynoides. — Nicholson. 
 
 One specimen of this genus was obtained at Loc. 26. It is smaller than any of the 
 figures of 0. calicularis. Nicholson,' and with only two 'teeth,' or prolongations of 
 the margin of the cup or calyx, instead of four or five, as described in the former, to 
 which it otherwise bears considerable resemblance. In each of the ' teeth ' may be 
 noticed a fine rod or fibre, which passes down into the substance of the polypaiy. 
 This structure has been noticed by Mr. Hopkinsonin the only other described species 
 of the genus 0. graeilis. Hopk.^ 
 
 Genus Climacograptus. — Hall. 
 
 Dieted vesicle in Climacograptus. — Amongst several scalariform individuals of a 
 species of this genus is one {M. 4528) with a short distal prolongation of the axis, ter- 
 minated by a small globular or pear-shaped vesicle.^ The whole polypary has been 
 converted into a white filmy material, but here and there the transverse slits or 
 apertures of the cells are visible. 
 
 Genus Diplograptus. — M^Coy. 
 
 Lateral fibres of Diplograpti. — A species of Diplograptus (M. 3888), somewhat 
 similar to that figured by Professor Mcholson in the first part of his Monograph,'' has 
 occurred in the present collection, but with the lateral fibres single. There are also 
 specimens allied to D. HarTmessi. Nioh.« (M. 3864, 3951, 3959), but-with the bifur- 
 cating lateral processes of the cells anastomosing and forming a network. These I 
 have provisionally called D. Harhnessi ? in the Sforegoing list, althou^ I presume it 
 is to such forms that Mr. Carmthers applied the provisional name of D. Bailyi,^ and 
 that Mr. Lap worth has founded his genus Lasiograptus.^ I am, however, not 
 acquainted with the typical species of the latter so as to institute a comparison. 
 Similar anastomosing fibres were observed by me in some specimens from the Lower 
 Silurian rocks of Victoria, Australia,' when I referred to their probable resemblance 
 to D. Bailyi. Carr. 
 
 Loc. and horizon, M. 3888, Loc. 26 ; M. 3864, Loc. 29 ; M. 3951, 3954, Loc. 27. 
 All from the Upper or Lead HOls Black Shale. 
 
 ^ We are indebted to Mr. Joseph Thomson, Gatelaw Bridge, for an opportunity of 
 examining the above specimens. 
 
 2 We are indebted to the kindness of Mr. H. B. Brady, F.G.S., for these deter- 
 minations. 
 
 3 Geol. Mag., iv., p. 108, t. 7, fp. 9-11. * Qeol. Mag., ix., p. 502. 
 ' Mon. Brit. Oraptolitidce, pt. 1, p. 70, f. 40. 
 
 ' Geol. Mag., iv., p. 262, t. 11, f. 6. ' Oeol. Mag., v., p. 131. 
 
 ^ Oeol. Mag., x., p. 659. ' Annals ifat. Hist., 1874, xiv., p. 5. 
 
51 
 
 Crustacea. 
 Trilobites in the Upper TJandeilo Rocks of the S. of Scotland. 
 
 Until the montli of April of last year (1874), Professor Harkuess was, so far as 
 known to tlie writer, the only observer who had discoyered trilobites in the graptolitio 
 shales of the Upper Llandeilo series of the S. of Scotland, when Mr. A. Macconochie, 
 Survey Collector, was lucky enough to hit upon a cast at Loc. 31 . Professor Harkness 
 announced the discovery of his specimen in a paper on the ' Lowest Sedimentary 
 Eocks of the S. of Scotland, ' read before the Geological Society of London in March 
 1856. It was found at Corfarding, near Tynron, parish of Penpont, Dumfriesshire, 
 and was referred to the genus Olenus.^ Professor Harkness was kind enough to for- 
 ward his trilobite to Professor Geikie on loan, and states in a letter (dated October 1, 
 1873), that ' it is not sufficiently well marked to make out satisfactorily what it is. 
 I think, however, that I was wrong in referring it to the genus Olenus ; it has more 
 the outline of Mncrinai'iis. ... I am more disposed to refer the specimen to this 
 genus than to any other.' The specimen is a cast in black shale of one-half the 
 pygidium, faint and badly preserved. 
 
 The trilobite found by Mr. Macconochie (M. 3948 A.)'is also a cast ezhibiting in an 
 ill-defined manner the thorax, pygidium, and a small portion of the carapace, and 
 appears to be referable to the genus PJiacopsf but the state of preservation is not such 
 that it could be referred to any described species. As, however, trilobites appear to 
 be so rarely met with in this portion of the SEurian series of Scotland, it appears to 
 me advisable to specifically distinguish it, and I have much pleasure in so doing after 
 its discoverer, Mr. Macconochie — Phacops ? Macconochii. 
 
 It may be well to state here, whilst on this subject, that Mr. James Bennie 
 obtained another trilobite (B. 3670 o.) from the Upper Silurian graptolitic shales, on 
 the E. side of Kirkcudbright Bay, in the autumn of 1874. This is referred to in the 
 succeeding note by Mr. Etheridge, F.E.S. I propose to call this Trinucleua? 
 Benniei. 
 
 NOTE ON THREE TRILOBITES FROM THE SILURIAN 
 ROCKS OF THE S. OF SCOTLAND. 
 
 The specimen from Corfarding, belonging to Professor Harkness, may be referred 
 to either of two genera — Cybile or Encrinurus, and I am disposed to refer it to the 
 latter genus. It is allied to E. sexcostatus rather than to E. punctatus. It is, how- 
 ever, very premature to attempt to name the specimen at all ; I am inclined to think 
 that it may be referred to the Llandeilo or Caradoc rocks, certainly not to any higher 
 group. 
 
 M. 3948a. — 1 can only provisionaUy refer this mould to the genus Phacops, 
 but for specific name the specimen is worthless. No characters can be made out. 
 Phacopidse occur in the Arenig and Llandeilo beds, somewhat resembling this form. 
 Probably the Llandeilo group may be referred to rather than Caradoc. 
 
 B. 3670c. This specimen absolutely shows nothing but the mould of a pygidium 
 of some trilobite, probably «■ Trinucleus. jEglina possesses a similar tail, and also a 
 broad and expanded head. The cephalic shield, in its present state, would do for 
 either genus, no punctse being recognisable, neither are there any body rings, or any 
 portion of the glabella. I cannot give any opinion as to the age of the rock from so 
 badly preserved remains. 
 
 The above three specimens must remain doubtful, none affording sufficient evi- 
 dence to determine (properly) their species or affinities. As before stated, they have to 
 me a Llandeilo facies. 
 
 R. ETHERIDGE. 
 
 28 Jbemtn Stkbet, 1st March 1877. 
 
 ^ Quart. Jour. Oeol. Soc, xii., p. 245. ' See Note by Mr. R. Etheridge, F.R.S. 
 
52 
 
 LIST OF PAPERS 
 Specially Illtjsteative op the Geology of the Area op Sheet 9. 
 
 The following list comprises only those papers having special reference to the ground 
 contained in this sheet. Of the more important of these a short digest is given, for 
 the purpose of showing the results obtained by previous observers. 
 
 1794. ' Observations on the Formation of Granite, ' by Sir James HaU, read March 
 1, 1790 ; Tram. Roy. Soc. Ed., vol. iii., p. 8. 
 In this paper the author states that he had been led to visit various parts of 
 Galloway, in order to examine the junction of the gi'anite and the schistus — 
 indicates the extent of the mass of granite to the west of Loch Ken, and the 
 nature of the junction between it and the schistus — points out that wherever 
 the junction is visible, veins of granite are seen running into the schists, vary- 
 ing from 50 yards to the tenth of an inch in width — infers that the granite 
 must, therefore, have flowed in a soft or liquid state into its present position, 
 and considers that these observations prove the truth of Huttou's views. 
 1815. ' On the vertical position and Convolutions of certain Strata, and their relation 
 with Granite,' by Sir James Hall, read Feb. 3, 1812 ; Trans. Roy. Soc. 
 Ed., vol. vii., p. 79. 
 In this paper the author endeavours to account for the convolutions of the 
 schists and greywackes by the intrusion of granite. Since 1790, he had 
 visited the mass of granite to the west of Loch Ken on several occasions, and 
 these observations confirmed his previous conclusions. He describes, in con- 
 siderable detail, the nature of the junction between the granite and the 
 schistus from the HiU of Lauren to New Galloway, indicating the best 
 marked veins of granite which occur at these localities. He infers that the 
 granite is posterior to the schists, and has flowed into its present position 
 from below upwards, in a liquid state. 
 1828. ' A short Sketch of the Geology of Nithsdale, chiefly in an economical point 
 of view,' by J. S. Monteath; Ed. Phil. Jour., vol. xix., p. 46. 
 A short description is given of the Closebum limestones, reference being 
 made to their thickness, chemical composition, and the character of the 
 fossils embedded in them. 
 1841. ' On the Sandstones of the Vale of the Solway and the formation of the Close- 
 burn basin,' by J. A. Knipe ; Brit. Assoc. Rep., vol. ix., p. 98. 
 Sketches the area of the Gtoseburn basin — points out that the new Red 
 Sandstone is the superior stratum resting on the Carboniferous Limestone, 
 while both lie unconformably on the greywaoke — notes the occurrence of trap 
 in the Cample "Water, which he supposes to be a basaltic dyke cutting across 
 the basin. 
 1843. ' Geognostical Description of the Stewartry of Kirkcudbright,' by E. J. Cun- 
 ningham ; High. Soc. Trans., new series, vol. viii., p. 697. 
 In this valuable paper the author gives a description of the different groups 
 of rock which enter into the geological structure of the County of Kirkcud- 
 bright—notes generally the character of the SUurian rocks, with reference to 
 their contortions, but attempts no classification of the different beds — indi- 
 cates the representatives of the lower stratified rocks found on the shore — 
 describes in detail the various masses of granite and their relation to the 
 transition strata, noting the granite veins, and the proofs of metamorphism 
 round the granite — calls attention to the occurrence of syenite, porphyry, and 
 trap in various parts of the Stewartry — briefly alludes to the connection 
 between the porphyry and the granite and syenite, regarding the one as a 
 mere mineralogical variety of the others, and inferring, from the nature of 
 their relations, that they must have had a contemporaneous and similar mode 
 of formation — notes the mineral veins occurring in the Stewartry. 
 1850. ' On the New Eed Sandstone of the Southern Portion of the Vale of the Nith,' 
 by Robert Harkness ; Quart. Jour. Geol. Soc, vol. vi., p. 389. 
 
 In this paper the author gives a detailed account of the Red Sandstones and 
 Breccias of the Dumfries basin — noting the localities where the beds are best 
 seen, and the general structure of the basin. He groups the beds in the 
 following order : — (1) The thick-bedded sandstones, with their overlying 
 
53 
 
 flaggy strata, about 130 yards in thickness ; (2) The conglomerate, 100 yards 
 thick ; (3) Fine grained soft sandstones, resting on the conglomerate, and 
 also ahout 100 yards thick. 
 
 1855. ' On the Anthracite Schists and the Fucoidal Remains in the Lower Silurian 
 
 Kocks of the South of Scotland,' by Professor Harkness; Quart. Jour. 
 Soc, Oeol. vol. xi., p. 468. 
 This paper contains a description of the section in Glenkiln burn, special 
 ' reference being made to the anthracite shales which occur at this locality, 
 and to the Banae flags, north of Dairy. The author places the Barlae flags 
 on the same horizon with the Grieston slates. A list of fossU fucoids, 
 zoophytes, etc., with notes, is appended to this paper. 
 
 1856. 'On the Lowest Sedimentary Eocks of the South of Scotland,' by Professor 
 
 Harkness ; Quart. Jour. Oeol. Soc. , vol. xii. , p. 238. 
 Indicates the position of the great Anticline, tlxe nature of the axial beds, 
 and fossils which have been obtained from them — abandons the theory, that 
 the parallel bands of black shale are repeated by faults, and adopts MurcM- 
 son's view, that they are brought up by folds — notes the occurrence of a 
 species of Olenus at Corfarding, near Penpont. 
 1865. 'On the Ancient Sea-beaches of the Mth VaUey,' by Dr. GOchrist ; Oeol. 
 Mag., vol. ii., p. 374. 
 The author considers the terraces on the right and left banks of the Nith 
 to be marine — states that marine shells have been discovered in the soil near 
 the brick works at the shooting range. 
 
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