and at the ferry over Pitt River it is about a mile across. Here it is less decomposed, showing hornblende crystals and generally a small amount of feldspar. It might be termed a hornblende granite. It decays to a great depth, and in this decayed mass are nodules and dike-like masses of fresh rock. From the mouth of the McCloud north to the United States fisheries, this hornblende granite appears in contact with dark semi-crystalline rocks, probably metamorphic, or with green granular rocks closely resembling intrusive diorite, but from stratigraphical relations shown near the Fisheries, it appears that it is a metamorphic sandstone. This hornblende granite is the rock referred to by Drs. White and Becker of the United States Geological Survey, as being older than the sandstones and slates underlying the Carboniferous. However, judging from the fact that the rock is generally fine grained near the edges, and ends in very irregular and ramifying dike-like projections, it seems that it must be intrusive and younger than the slates. From the mouth of the McCloud up Pitt River the rocks are all crystalline, or nearly so, until about a mile and a half below Silverthorn Ferry, where highly metamorphic and contorted sedimentary strata are met; strike a little east of north, dip a high angle to the east. The crystalline rocks consist of amygdaloidal diabase, diorite, and porphyries, with massive green rocks of indeterminate composition. A body of iron ore outcrops on the north side of the river. It shows a heavy gossan capping and scattered bunches of magnetite. Northward along the western slope of the lime stone mountains the iron ore is thickly scattered over the surface. It is said to occur in great quantity in places. Several small developments have been made and ore shipped. The ore lies near the contact of the limestone with the eruptives. The deposit is very similar to that near

Stillwater.

The scenery is very picturesque about the United States fisheries. The McCloud is a clear, cold stream of great volume, rising in Mount Shasta. On the east there extends for many miles a high and rugged limestone range, known as the Gray, or McCloud Mountains. The geological features about here are varied and of great interest. Car boniferous fossils are quite abundant, and there is a large variety of intrusive and metamorphic rocks. A short trip was made up the river, and the mountains on the east climbed until the limestone was reached With scarcely any exception, the series of rocks exposed between the limestone and the river is intrusive. Near the river is a fine-grained diorite, then a brecciated porphyry, changing to a quartz feldspar por phyry. Above this are dikes of diorite, narrow strata of metamorphic rock, and amygdaloidal diabase, in the order mentioned. The limestone rests on these intrusives and stretches out long, narrow arms down the mountain to the west. Between the arms are bodies of diorite. The limestone dips northeast to east, with greatly varying angles. At one place it is not over 30°, at others nearly vertical. Whitney states that the thickness of the limestone is 1,000 feet, but I believe it is much greater, probably twice that amount. At the southern end of each of the main peaks the strata seem to have been crushed upward from the south. On the western side of the range the debris from the cliffs has been cemented by percolating lime water, so as to form extensive tufa 20 to 30 feet thick. Judging from the manner in which the lime stone has been broken up, the crystalline rocks underneath are cer tainly younger. Fossils are scarce in the main body of limestone at

this point. Large caves are said to exist in this limestone range, but time did not permit of their exploration. A half mile below the Fisheries the hornblende granite terminates. It is succeeded northward by diorites and feldspar porphyrites, with some greatly altered metamorphic rocks, showing a steep dip to the northeast. It seems to penetrate the semi-crystalline rocks and become fine grained on its edges, with generally a sharp contact. It is quite probable that this rock is the upward termination of a large body of granite, to which the extreme metamorphism of the sedimentary rocks is due. A little below the Fisheries a gulch comes in from the west, and it is seen that the intrusives are soon replaced in that direction by sandstones, argillites, and grauwackes, in such a highly metamorphic condition that the stratification is not often seen. The metamorphism grows less toward the west, and in the course of a mile we reach soft shales and blocky slates, with a strike a little west of north and variable dip toward the east. Black slates appear on the Sacramento River road a mile west of the Fisheries; strike east and west, dip 15° north.

The sedimentary strata about the Fisheries are very highly metamorphosed, and it is frequently difficult to distinguish them from the dikes of diorite and diorite porphyrite which occur here. Just above the Fisheries, on the west side of the river, there are dark, argillaceous, fossilbearing strata, rather thick bedded. These contain disconnected layers of impure limestone; strike a little west of north, dip 30° to the east. The argillites and not the limestones are fossiliferous here. A few yards to the north, these fossiliferous rocks become jointed and highly metamorphosed, blending downward across the strike into rocks that become pyritiferous and very compact, then more feldspathic and granular, while the northernmost exposure is a massive heavy diorite. It is very difficult to say whether there is a direct continuation downward of the fossiliferous strata, which become more and more crystalline, or whether it is a dike, whose junction with the metamorphic rocks can not be seen on account of similarity of appearance. At the southern end of the argillite outcrop is a slightly porphyritic diorite, whose eruptive nature is unquestionable on account of the sharp contact which it shows. Argillitic rocks, frequently containing fossils, occur along the trail which leads up the river to Campbell's place, 8 miles above. There is much similarity, both in the character of the strata and in the fossils. Dikes of diorite and strata of quartzose and of feldspathic composition separate the fossiliferous beds. The rocks are in great part metamorphic, but the bedding is not prominent. The slaty rocks strike north 20° to 60° west, and dip from 30° northeast to vertical. Thin beds of limestone are associated with these rocks, but they do not carry fossils. The limestone peaks along the east side of the McCloud River extend in a north and south direction, but the strike of the formation is generally northwest and southeast. The repetition of the limestone bodies in a north and south direction, as well as that of the fossiliferous beds along the river, is undoubtedly due to sharp folding or faulting, whereby the same strata are repeated several times. If this were not so the thickness of the limestone would be immense. The limestone mountains were climbed south of Campbell's and found to be underlaid and cut up by dikes of diabasic rock. Radial arms of limestone extend down the mountain from the main ridge in every direction, and are often entirely isolated by the intrusive rock. At one place a purplish, faintly por

phyritic rock underlies the limestone. It, with some other rocks much jointed and shivered by dynamical action, seems to have been left adhering to the limestone when it was caught in the intrusive masses. Considerable local variation exists in the strike and dip of the limestone; dip from nearly level to a high angle to the northeast. Fossils are reported to be abundant on the mountains 2 miles south of Campbell's, but the locality could not be found.

The formation is well exposed along Campbell's Creek. It appears to be pseudo-diorite and other highly metamorphosed rocks. These rocks extend to the divide on the east, slates not appearing till Squaw Creek is reached. One mile east of Campbell's the slates strike north 50° west, dip 45° northeast.

The McCloud through the greater part of its course flows with a swift current between steep, and often rugged, but not precipitous, mountains, with scarcely any bottom land. Timber is not abundant on the mountains, and what there is is largely oak. About a mile above Campbell's the course of the limestone carries it across the river. It appears in detached bodies for some distance up to this point. West of the river it rises in a high ridge for several miles, then in a second one, while on the east side of the river, opposite, and about 6 miles above Campbell's, are other high limestone peaks. The country rock continues to be a green stone to a large extent, often certainly of sedimentary origin.

About 9 miles from Campbell's, on the north side of the river, the limestone occurs in thin strata, alternating with hard, green or purplish rocks; dip 55° northeast. On the south side the dip is half that. It is overlaid by conglomerates, quartzites, and other granular semi-crystalline rocks. Underneath are argillaceous rocks, filled with imprints of branching forms (bryozoa). This is the last of the limestones on the McCloud. The beds extend off in a northwest direction, toward the head of Hazel Creek. On the divide they form a high mountain, rising fully 6,000 feet. Twelve miles north of Campbell's the rocks are chiefly greenish to purplish conglomerates, very hard and compact.

East as far as the divide separating the McCloud from Squaw Creek, there is much hard metamorphic rock, with quartzites and greenish semi-crystalline, fragmental rocks, together with some probably intrusive. In the hills just south of the river, 12 miles above Campbell's, there is an outcrop of a dark calcareous argillite, rich in fossils. The strata dip to the east 30° and strike a little west of north. They are about 3 miles east of the limestone. The fossils are probably Carboniferous. Rocks similar to these described outcrop along the river to the north of Chatterdown Creek. Up the creek appear green conglomerates, slates, diorites, and thin-bedded quartzites. The latter occur in very regular strata, a few inches to a foot thick, with thin, soft argillitic layers between; strike north 40° west, dip 65° northeast. Eastward appears a green rock, often fully crystalline, often conglomeritic with pebbles of eruptive rocks, porphyries, and porphyrites, sometimes amygdaloidal. Judging from the pebbles in the creek, black slates must outcrop toward the head of the creek. The great mass of the rocks are semi to fully crystalline, and generally massive. This is a very interesting field for the study of metamorphism. Nothing certain can be said until a microscopic examination has been made. It is certain that there are some intrusive rocks in this region, but the origin of most of the massives is in doubt.

Petrosilex is another common rock. One mile south of the mouth of Chatterdown Creek is a purplish porphyritic rock. Fossils are reported from limestone at the head of Chatterdown Creek, but the locality was not visited. The McCloud has an elevation of 1,300 feet at the mouth of Chatterdown Creek. The mountains rise about 2,000 feet more, with occasionally higher peaks. The mountains are very brushy and it is almost impossible to travel over them, except on the trails. Between this point and Campbell's the river is bordered in many places by one or two terraces of water-worn pebbles, the highest one sometimes being 200 feet above the river. Near where the river cuts across the limestone above Campbell's is a red porphyritic rock, resembling that seen under the limestone farther south.

The presence of quartzose rocks and conglomerates associated with the McCloud limestones, generally overlying, would in itself indicate a different geological horizon from that of the limestone on Squaw Creek, which is almost exclusively associated with slates.

Many of the conglomerates or tuffs contain green, dark red, or purplish pebbles, similar in appearance to the massive rocks, but no non-conformity is apparent in the whole series, so that it is not likely any formation which now appears could be the source of the pebbles. The coarse conglomerates generally overlie the limestone, while quartzite and sandstone occur on both sides.

Between the mouth of Campbell's Creek and the Fisheries, on the east side of the river, fossils are frequently seen. At one spot imperfect trilobites were obtained. Three miles above the Fisheries a cherty limestone was seen, with a strike nearly east and west.

Soft shales become the prevailing rock one and a half miles west of the Fisheries. They are cut by many dikes of diorite, and farther west by diabase. Although very irregular in strike and dip, there is certainly no break between these shales and the highly metamorphosed rocks on the McCloud.

It is to be noted that the apparent slight degree of metamorphism shown by the shales is no sure indication that they have not been subjected to metamorphosing influences, for in many cases, action which will harden quartzose rocks and sandstones will have apparently but little effect on clayey rocks, owing to their impenetrability. In addition, slates and shales soften near the surface, while more quartzose rocks maintain their solidity.

Near the summit we find the shales in contact with hard sandstones, which are almost metamorphosed to quartzites. On Salt Creek is a body of quartz feldspar porphyry, in the decayed portions of which the idiomorphic crystals stand out finely. The summit of the divide is 1,600 feet. At the Sacramento bridge it is 1,100 feet.

The western slope of the hills forming the divide is very barren; the trees are few, and the soft shales decay and wash away so easily that in many places even brush does not grow. For some miles after leaving the McCloud the shales strike in a north and south direction, dip east, and as the Sacramento is approached they strike east and west, dip north at a small angle. Near the bridge they are greatly broken and crushed. They are chiefly black slates, with frequent strata of dark quartzite and quartzose conglomerates. They assume all positions in strike and dip in the course of a few rods.

The Quaternary gravels on which Redding is situated give place,

about a mile up the Middle Creek road, to small outcrops of sandstone, probably Cretaceous. This is followed by the Auriferous Series, which outcrops along the river for about a mile south of Middle Creek. It consists largely of massive rocks, dark and fine-grained, and often showing faintly amygdules of calcite and other minerals. The rock varies from chlorite schist, through dark intermediate varieties, to a syenite with distinct hornblende crystals. The greater part is intrusive, but there are places where there is a distinct sedimentary structure; strike north and south, dip 80° to the east. Along Middle Creek there are good exposures, and the eruptive nature of at least a part of these rocks is shown. Fig. 2 shows an irregular dike, which is scarcely distinguishable from the rock it intersects, save for its strongly marked boundaries. A peculiarly faulted quartz vein lies near it. This dark rock gives place to a coarse granitic one with large quartz veins, chlorite, and a little feldspar. The granite appears perfectly massive, though showing the effect of great crushing. It begins as bunches and ramifying dikes and finally becomes the country rock. It extends along the creek as far as Shasta. It is sometimes replaced by dark chloritic dikes. Irregular and bunchy quartz veins are to be seen, and in these prospecting has been done. The granite is very rich in quartz, and though no fresh hornblende appears in it here, yet from the shape of the chloritic bunches, they were undoubtedly derived from hornblende; making the rock originally a hornblende granite, undoubtedly of an intrusive nature, but at present reduced to the extreme stage of decomposition. As before mentioned, this rock is identical in character with that at the ferry on Pitt River. South of Shasta this granitoid rock contains less feldspar and more chlorite, forming a massive, dark green rock, rich in quartz. There is no apparent bedding, but occasional strata of softer rock; strike north 25° east, dip 80° southeast. Near Centerville, and from there westward, the rock shows plainly a strike north 65° west, dip 80° northeast. Two miles south of Shasta is the Thompson Mine. There is a large vein here, carrying rich sulphurets and free gold; direction north 20° west, dip 45° northeast.

At Centerville is an old river channel running nearly north and south. A shaft of 100 feet has not touched bottom. Bedrock appears on both sides, giving a channel between 200 and 300 feet wide. In the early days Middletown and Centerville were towns of considerable size, supported by extensive placer diggings, but now their locations can hardly be recognized. South of the Muletown Mountains the rocks are metamorphic schists; strike north 75° west, dip 80°

north. About Muletown there is an interesting series of formations to be studied. Extensive and rich placers were worked here in the early days, but as yet no extensive quartz mining has been successfully undertaken. On the northern end of the mountain the rock is similar to that south of Shasta. In places it contains but little chlorite, and blends toward the south into an almost pure massive quartzite. More study is necessary to determine the relation between this apparent quartzite and the chlorite granite. Hornblendic, chloritic, and talcose schists replace this rock on the southern end of the mountain; strike often a little south of west. On the western side of the mountain are dikes of a beautiful porphyritic diorite. These have a north and south direction. Similar dikes are also found on the northeastern side of the mountain. The porphyritic diorites on the west slope have been intruded in the quartzites, which narrow to a point toward the south, and which have on the east, running nearly north and south, dikes of syenite and lightcolored quartz porphyry. The dikes are followed southward by dark massive felsitic rocks, while syenite occurs on the west. Just south of Muletown is an outcrop of micaceous syenite. Between this point and Clear Creek nothing but syenite is seen, and it also appears to be the prevailing rock over a considerable extent of country west of the creek, but is separated from the granitic diorite of Mount Bally by a considerable width of metamorphic rock. One half mile south of Muletown all the bodies of intrusive rock are replaced by slates and light-colored talcose schists. The main quartz veins of this district run north and south. Nearly all the surface on the western slope of the mountain down to Clear Lake was very rich in placers. One principal vein, running north and south over the mountain, is traced for some distance at the contact of syenite and quartz porphyry. West of it is a vein in the syenite and on the flat at the foot of the mountain are other veins, either in the syenite or at the contact with a stratum of hornblendic rock. These veins dip east at a very high angle. The main vein after it leaves the syenite continues across the southern end of the mountain in the schists, cutting them at a large angle and preserving a constant course. These veins are developed only by surface work, except in two instances, where tunnels of some length have been run. The ore is mostly sulphurets, with little free gold below the water line. The region has been a favorite one for pocket hunters. The sulphurets are rich, but there is no extensive development to show the real character of the district. On the north end of Muletown Mountain a rich east and west vein occurs. In the syenitic granite just south of Muletown, for a distance of over 100 feet east and west, there are minute parallel veins of quartz, one eighth to one and a half inches wide, which strike north 80° west. They dip west 85°, and are remarkably even and regular. The veins are from 4 inches to 1 foot apart. Some show a decay of the syenite along each side with a little appearance of. slickensides, indicating a fissure; while others are frozen to the rock Some seams parallel to these show polished sides and no quartz. As the quartz weathers out, the syenite, though perfectly massive, assumes the appearance of a bedded rock. Some cross cracks exist, which in one case has caused a vein to jump; not a faulting of the rock, as the adjoining veins are not disturbed. (Fig. 3.) These are barren, though irregular and bunchy veins near by contain gold. A compact conglomerate appears about 2 miles north of Horsetown, in the sides and

bottom of the gulches. This is formed of the various rocks which go to make up the southern end of Muletown Mountain. It dips southeast at an angle of 15°, and in that direction is gradually succeeded by sand stones. A minute quartz vein appears in this conglomerate, filling a crack which has been formed since its solidification, for the vein follows a direct course through pebbles and matrix.

Sandstones, nearly horizontal, and containing some fossils, outcrop on Jackass Flat, a little south of Centerville.

North and west of Horsetown there is a small outcrop of granite. A brown sandstone rests on the granite. It is inclined east at an angle of 20°, and contains numerous fossils, among which are ammonites. This is the locality from which the Horsetown beds were named. They con stitute the next to the lowest division of the Cretaceous in this State The fossils occur in concretionary nodules.

Horsetown is another example of the early mining town, once sustained by the placers, but now entirely gone to decay. One mile east of Horse town, on the north side of Clear Creek, is an outcrop of the Metamorphic Series. It consists of fine, cleavable, and highly altered slate inclosing a body of gray limestone. The strike is north 30° west, dip 40° to the east The limestone appears to be not over 100 feet thick and lenticular in shape, as it outcrops for a few hundred feet only. A number of faint coral forms were gathered; they weather out on the surface. Lime has been quite extensively burned here at some period. A short distance west of the limestone the slates strike 65° west, and are quite talcose. South of Clear Creek the country is entirely covered with stratified gravel deposits, sloping gently toward the Sacramento. The streams have worn shallow valleys in them. North of the creek, where the gravel are shallow, much placer mining has been carried on. A half mile west of the limestone the strata dip 30° to the east, but between Horse town and Centerville, wherever exposed, the dip is very steep.

Going east from Centerville we soon strike a porphyritic diorite sim ilar to several of the dikes on Muletown Mountain. Occasionally strata of green schistose rocks occur in it; strike north and south, dip east This diorite outcrops along the road 2 miles, though I do not think i extends far north and south. On the east it is finally covered by Cre taceous sandstones, rich in fossils, which dip southeast at a small angle The sandstone does not extend far until it becomes covered by the Quaternary gravel.

The Old Diggings and Churntown districts, north of Redding, were not examined as extensively as some other portions of the county, for the reason that a lengthy report was given of them in the last annual publication of the Mining Bureau.

The line of hills which border the Sacramento River on the east between Redding and the mouth of Pitt River, belongs to the Auriferous

Series, and the rocks are well deserving of that designation. The gulches leading both east and west from this ridge were very rich in gold, but now the chief interest in this section centers in the numerous goldbearing quartz ledges. The Churntown district lies on the east, and the Old Diggings on the west. Both are very similar in regard to geological structure and in character of ores, though more silver is to be found in the eastern side. This line of hills seems formed of parallel dikes of fine greenish, crystalline rocks and greatly altered quartz and feldspar porphyries. Between them are strata of highly altered sedimentary rocks. Both dikes and slaty rocks have in general a strike a little east of north and west of south, and a very steep east or west dip. The ore is sulphurets and free gold, with generally very little silver. The veins occur at the contact of porphyry with slaty rocks, of two different kinds of porphyry, or of porphyry with massive greenish dikes, which are so decomposed that no precise name can be given to them. In some of the mines the ore is chiefly sulphurets, in others part sulphurets and part free gold. Owing to the uniform strike of the dikes and country rock in the Old Diggings district, the veins are regular and have the gold distributed quite evenly. The mines in this district are improving with depth, and it can be safely said that they are true fissure veins. The Texas Consolidated Mine is one of the deepest, being down at the time of my visit 640 feet. The vein sometimes reaches a width of 14 feet, with good fissure walls. Three veins are worked in this mine. They contain no barren quartz.

The Calumet Mine is one of the southernmost in the district. The vein strikes a little east of north, and dips east 60°. The walls are part slate, part porphyry. The vein crops for nearly a mile and is supposed to be identical with one of the main veins farther north. The gold is largely contained in iron sulphurets. The free gold is very fine.

The bedded rocks exposed along the railroad between Middle Creek and Mr. Paul's reduction works show a strike of north 10° to 30° west, dip usually west. The rocks do not cleave well, but are joined and show polished seams. There are several dikes of a handsome syenite porphyry. There are also many greenish dikes, which are so altered that it is impossible to discover their original composition, and it is often difficult to distinguish between them and the metamorphic rocks. Amygdules of calcite and epidote are thick in places, and they are good indications of the rock's origin. Many quartz veins appear, sometimes at the contact of the schists with the eruptives, and sometimes in the eruptives.

Judging from the amount of alteration, the dikes represent two periods; the porphyritic dikes are in all cases the younger; the older are compact, fine grained, and possess a green color. They are either massive or schistose.

Here

The surface rock under the gravels is often decayed down 25 to 40 feet. Hence, the time must be great since their surfaces were exposed to erosion. This period probably antedated the deposit of the great body of gravels and conglomerates filling the head of the Sacramento Valley. The Eureka Tellurium Mine is located near Middle Creek. tellurides of gold and free gold were found in a shaft sunk 70 feet. A tunnel has been commenced to tap the vein 100 feet below the shaft. The rock in the tunnel is fresh and undecomposed. It is partly a chloritic petrosilex, and partly an aphanitic diorite. In the diorite is a

dike of syenitic feldspar porphyry. The great majority of the dikes in this section follow the strike of the Metamorphic Series.

South of Middle Creek, and a mile southeast of Shasta, are some hills having as their center syenite and chloritic diorite. The chlorite granite to the east and south is filled with small, irregular gold-bearing quartz seams. Much surface work has been done on these little veins in the search for pockets. Bands of dark rock extend through the granite in an east and west direction. A little southeast, in Sec. 5, T. 31 Ñ., R. 5 W., is a prominent vein, exposed in a direction north 18° east on the crest or western side of a line of hills; the dip is 70° east. The vein is known as the Oro Fino. The hanging wall is diorite, the foot talcose schist. The southern end of the vein is in Section 8. It terminates very abruptly in a great mass of quartz on the summit of the hill. The northern end is covered by gravel. The ore consists of iron and copper sulphurets and fine gold. A short distance to the west is a series of veins in chloritic schist, and running a little west of north. The Silver King Mine is located in the same township, Section 9. The ore is antimonial silver in white quartz.

West of Shasta there are no dikes, as mentioned by Professor Whitney; simply the white granitic rock so extensively developed east of the town. It has little chlorite and closely resembles arkose, consisting of quartz and feldspar in a granular form. The toll road runs over a hill, 2 miles west of Shasta, which is formed of a white quartz porphyry so greatly altered that its true nature is hardly recognizable. Its intrusive origin is shown by the almost perfect idiomorphic form of many of the quartzes. This porphyry mass is over a mile wide. In the center is a stratum of schists. West of the porphyry, and extending several miles past Whiskytown, is a green rock, often semi-crystalline and varying from massive to schistose. It is not certain whether this lamination is that of sedimentation or that of pressure. The strike is north 40° to 50° west; dip, a high angle to the northeast. The hills on the north are brushy and show no crystalline rocks, save an old amygdaloid. Two miles east of the Tower House a crystalline rock outcrops along the road and in the hills on the north. It has a feldspathic ground mass, in which are thickly imbedded green hornblende crystals, also some quartz. It is probably a diorite, but is not well differentiated from the semi-crystalline rocks adjoining on the east. At one spot a dike of quartz porphyry occurs in the green schists. These schists belong to that class of rocks very numerous in Shasta County, whose origin is doubtful. Much more study is necessary to determine the question. Black, finely cleavable slates outcrop three fourths of a mile east of the Tower House; strike north 50° west, dip 70° northeast. Mill Creek flows into Clear Creek at the Tower House. Up that creek the slates are soon replaced by feldspathic and chloritic schists, and at a distance of 2 miles by a micaceous diorite, often gneissoid.

Down Clear Creek the slates become hard and blocky. A careful search in the slate about the Tower House did not reveal any fossils. One mile north of the Tower House the slates dip south, and are followed by conglomerates of slate and silicious pebbles. The slates are so highly metamorphosed that they ring on being struck. There is no quartz mining in the vicinity of the Tower House, but the placers have been found very rich along Clear Creek. The Tower House has an elevation of 1,330 feet.

The rock exposed along the more northerly of the two toll roads leading over the Trinity Mountains is almost wholly slate for 4 miles; strike 40° to 50° west, dip northeast. The slates finally become irregular in strike and dip, and are followed by silicious conglomerates nearly to the summit, when granite appears. Only one dike, a porphyritic diorite, was seen on this road. Green massive silicious rocks outcrop along the southern road for 2 miles west of the Tower House. Then there is about a mile of black slate not greatly altered, being soft and jet black. Three miles up this road dioritic granite appears. In its vicinity the black slates are partially metamorphosed, having a minutely wavy surface, caused by the development of small needle crystals. This appearance is noticeable for a hundred feet or more around the granite. A harder slate follows for a quarter of a mile. Near the main body of the granite the slates strike north 60° west, dip 65° northeast. The exact contact cannot be seen here, but coarse dioritic granite seems to terminate abruptly against the slates. There is no doubt, whatever, that the granite has been intruded through the slates, and is consequently younger. Slates appear again along Clear Creek, a little south of French Gulch; they dip north 40° to 60°, strike east and west with great variations. The rocks exposed along Kline's Gulch, which leads up to the Gladstone Mine, are slates and fine silicious conglomerates. The strata turn and dip south 70° to 80° at the Gladstone Mine, and in general the dip of the veins is the same. The walls of the vein worked in this mine vary greatly, sometimes black shining slate, at others silicious conglomerates or fine-grained silicious slates. In many places there are bunch-like bodies, or narrow irregular bands of a light green feldspathic dike, probably once a diorite. The regularity of the fissure at this place is undoubtedly due to the presence of this dike, for the country is so broken that it is hardly possible that a well-defined vein could exist for such a distance as is here shown. Polished quartz and clay seams are characteristic, with a general ribbon character of quartz. The ore is worked for free gold and sulphurets, which are rather fine. The sulphurets occur in black layers and bunches in the quartz. The Gladstone Mining Company owns a number of claims along this series of veins, and have opened a continuous body of quartz 1,900 feet in length, and a depth, as far as exposed, of 900 feet. This depth is measured from the top of the hill to the lowest tunnel. The greatest width of the vein is 22 feet; average width, 4 to 5 feet. The greatest amount of work has been done 700 feet below the top of the hill. The Gladstone Company owns 8,500 feet of claims. On the west there are over 3 miles of claims located on this same series of veins. The mountains are high and the gulches steep and narrow, so that but little pine is found.

A second examination was made of the arcose-like rock west of Shasta, and it was determined to be a quartz porphyry, whose character was masked by the crushing which the quartz crystals have undergone. They are often drawn out in lenticular forms, arranged parallel. Some are half an inch long and full of cracks. The unbroken ones still show plainly the crystal facets. A half mile west of Shasta is a large body of diorite, followed eastward by the chlorite granite before described. In many places the granite differs from the quartz porphyry just described, by a greater amount of chlorite and less feldspar. The granite appears for 3 miles along the road to Iron Mountain. There then appear strata