M axim a of the intensity of the solar radiation at various regions of the earth's surface. L.
G o r c z y ń s k i (Rev. Chim. Pura Appl., 1931, [iii], 6, 1— 15).—Max. vals. of the solar radiation, for tropical ocean, ocean in temperate zone, on land at or above sea level, and in the upper atm. are recorded. The low vals. at sea level are due to absorption by H 20 vapour; this effect is noticeably greater in the tropics. H. F. G i l l b e .
Physico-chem ical constants and radioactivity of the w ater of Corgas [Portugal]. P. F o r j a z
(Rev. Chim. Pura Appl., 1931, [iii], 6, 15— 16).—The H20 contains 0-2404 g. of solids and 13-1 c.c. of N 2 and inert gases per litr e ; traces only of H C03', Fe, and Mg are present. Its radioactivity is 0-61 milli- microcurie per litre. Various physical consts. are
given. H. F. G i l l b e .
Relation between com position of m ud and of S alt Lake brine. V. I. N i k o l a i e v (J. Appl. Chem.
Russia, 1931, 4, 627—632).—Mud of the salt lakes gradually adsorbs CaS04 and Ca(HC03)2, K salts, and Br,” but not Na*. C h e m i c a l A b s t r a c t s .
Origin of diam ond in the South and West African coasts. E. R e u n i n g (Neues Jahrb, Min., 1931, A, 64. Beil.-Bd.. 775— 828; Chem. Zentr., 1931, ii, 3455).
A nalysis of a Canadian cyrtolite. 0. B.
M u e n c h (Amer. J. Sci., 1932, [v], 23, 273).—A sample from Ontario contained 0-529% U, 0-431%
Pb, and 0-08% Th, whence the age of the mineral is calc, to be 571 X 106 years. C. W. G ib b
i'-M elting of granite. R. W. G o r a n s o n (Amer. J- Sci., 1932, [v], 23, 227—236).—Granite from stone Alt., Atlanta, Georgia, becomes completely liquid (apart from haematite) at 700 ± 5 0 ° in the presence of HP0 vapour at a pressure of 980 bars. The liquidus of the dry granite is calc, to be at 1050±50°.
C. W. G ib b y .
Occurrence of iron ore in M inas Geraes, Brazil.
E. A. S c h e i b e (Arch. Eisenhiittenw., 1931—1 9 3 2, 5, 391— 406).—The geology of the Fe ore deposits between Queluz and Bello Horizonte is discussed in detail. In the primary deposits there are two distinct types of ore, viz., (a ) pure itabirite consisting of
stratified red haematite with >68% Fe and <0-03%
P containing local inclusions of magnetite, and (b)
micaceous Fe schist consisting of finely-handed massive deposits of thin layers of specular Fe ore interspersed with quartz and containing 45% Fe with 0-02% P. The only important secondary ore is the so-called “ canga,” which consists of a relatively thin conglomerate or glassy layer of ferruginous minerals containing 60% Fe and <0-2% P. The southern portion of the deposit contains much dolomitic limestone and high-grade Mn ore. In some parts there are thin intrusive seams of eruptive rock containing Au. A. R. P o w e l l .
Constitution of oolitic m inerals [of Lorraine].
J. P. A r e n d (Compt. rend., 1932, 194, 990—993;
cf. this vol., 360).— 11 analyses are given of the oolitic and gangue portions of four vertically suc
cessive beds, and of the pisolitic, oolitic, and gangue portions of the pea-ore (Bohnerz). The relative proportions of oolite and gangue in each are also stated. The variations depend mainly on the acces
sibility of 0 2 to the various beds. The changes are accompanied by an increase in d and consequent diminution in vol. C. A. S i l b e r r a d .
A v e r a g e c h e m i c a l c o m p o s i t i o n o f d i f f e r e n t r o c k t y p e s . A. J o h a n n s e n (Jahrb. Min. Beil.-Bd., 1931, 64, 505—516; Chem. Zentr., 1931, ii, 3196).—
A division of rocks into 4 classes w ith subdivisions.
L. S. T h e o b a l d .
Mineralogy of B razil. Occurrence of anatase, zircon, and a vanadium niobate in N . Brazil. E.
R e m a n n (Jahrb. Min. Beil.-Bd., 1931, 64, 423—
436; Chem. Zentr., 1931, ii, 3196).—Anatase, zircon, and a vanadium niobate (ochre-red in colour, strong lustre, and high refractivity), probably of Y, were isolated from an opal. The spectrum showed strong lines of Y in addition to those of V and Nb. La, Ce, Ta, and weak U and Pb lines were also present.
L. S. T h e o b a l d .
Zeolite m inerals of the basalts of the Platten Lake region in H ungary. B. M a u r i t z (Jahrb. Min.
Beil.-Bd., 1931, 64, 477—494; Chem. Zentr., 1931, ii, 3196).—Phillipsite, apophyllite, chabasite, thaum- asite, heulandite, natrolite, and calcite were found in the rock-cavities. L. S. T h e o b a l d .
S t e e n s t r u p in e . F. M a c h a t s c h k i (Jahrb. Min.
Beil.-Bd., 1931, 64, 235—250; Chem. Zentr., 1931, ii, 3195—3196).—Steenstrupine has a : c 1 :1-0836;
the structure is not similar to that of eudialyte. The formula is X 3YZ3(0 ,0 H ,F )12, where X is Na, Ca, Ce, La, and Di, Y is Mn", Mn"', Fe'", Al, and Z is Si and P.
Powder photographs give a 9-47, and c 15-39 A., whilst rotation photographs give average vals. of
a 9-64 and c 15-25 A. The unit cell, wt. 4195 X 10'24 g., d 3-31, has 5 units of the above formula. Attempts to recrystallise altered steenstrupine occurring in the metamictic condition failed. L. S. T h e o b a l d .
C om position of g a rn ets. B. G o s s n e r (Jahrb.
Min. Beil.-Bd., 1931, 64, 225—233; Chem. Zentr., 1931, ii, 3195).—Deviations from the normal ratio Si02: M"0 : M"20 3 in certain garnets are discussed.
Almandine from Dillenberg, near Neu-Albenreuth, has the composition S i0 2 37-00, A120 3 20-36, Fe20 3
2-09, FeO 30-80, MnO 7-57, MgO 1-52, and CaO 0-98%; d 4-232. Melanite from Fraskati has the composition S i0 2 35-08, A120 3 4-77, Fe20 3 21-37, FeO 2-10, T i0 2 3-60, CaO 33-10, MgO 0-39, and MnO
0-41%. L. S. T h e o b a l d .
Aragonite from the rock-cavities of the lower Rhine basalts. K. O b e n a t j e r (Jahrb. Min. Beil.- Bd., 1931, 64, 437—442; Chem. Zentr., 1931, ii, 3195).—Crystallograpliic measurements of 50 aragonit e crystals gave (4, 13, 0), (140) (150) (160) and (350) as new, mostly vicinal, faces. L. S. T h e o b a l d .
Pseudoabsorption. F. C o r i n (Bull. Soc. frang.
Min., 1931, 54, 57—63; Chem. Zentr., 1931, ii, 3194).—Pseudoabsorption in calcite appears to be a complicated process due to other properties besides polarisation, reflexion, and refraction. A calcite from Eysden showed strong pleochroism (brownish- black to colourless) which is traceable to very fine inclusions, probably of argillaceous matter.
L. S. T h e o b a l d .
Sim ple sliding of anorthite. 0 . M u g g e and F.
H e i d e (Jahrb. Min. Beil.-Bd., 1931, 64, 163—170;
Chem. Zentr., 1931, ii, 3195).—Numerous thin laminae were formed about (010) when homogeneous, regular, twinning-free crystals of anorthite were embedded in clay or N aN 03 and submitted to pres
sures of approx. 25,000 kg. per sq. cm. The striations are anomalous and indicate a simple sliding process.
L. S. T h e o b a l d .
Rare m inerals in pegm atite, Pointe du B ois, Manitoba. T. L. W a l k e r (Univ. Toronto Stud.
Geol. Ser., 1931, No. 30, 9—13).—The triphylite contained : Li20 8-36, Na20 0-12, K 20 0-44, H 20 0-99, MgO 0-23, CaO 0-65, FeO 21-70, MnO 21-13, P 20 6 46-41, insol. 0-20%. The columbite contained FeO 14-77, MnO 2-17, CaO 2-66, MgO 0-45, Nb20 5 52-26, Ta20 6 26-41, T i0 2 0-49, S i0 2 0-13, Z r02 0-65, H 20 0-21%. C h e m i c a l A b s t r a c t s .
Lattice dim ensions of certain m onoclinic am phiboles. G. G r e e n w o o d and A . L. P a r s o n s
(Univ. Toronto Stud. Geol. Ser., 1931, No. 30, 29—
39).—Pargasite (from Pargas, Finland) has a 9-88,
b 17-70, c 10-92 A .; hornblende (from Anakie, Victoria) has a 9-88, b 17-85, c 5-443 A. There are at least 2 types of end-members for the monoclinic amphiboles:
a pure meta- and a pure ortho-silicate. In certain specimens in which the unit cell is doubled along the c axis, double-salt formation between meta- and ortho-silicate is postulated.
Ch e m i c a l Ab s t r a c t s.
Ortboclase lavas of the volcanoes of Tibesti.
A. L a c r o i x (Compt. rend., 1932, 194, 757—761).—
Throughout the massif of Tibesti the oldest and newest lavas are basaltic, those of intermediate age are leucocratic. The orthoclase varieties of these last include rhyolitoids containing numerous splier- ulites. They are rich in alkali, and include com- endites, d 2-395, and pantellerites, d 2-420, passing into trachytes; elsewhere occur microgranites and an obsidian rich in fayalite, and also calco-alkaline rhyolites containing in places much bronzite. The phonolites include varieties containing segyrine and/
or nepheline. Among the trachytes occur a latite, and a rock resembling doreite. The dyke rocks
494 B R I T I S H C H E M IC A L A B S T R A C T S .— A .
include a microsyenite closely resembling rhomb - porphyry, a micro-akerite, and (probably) two rocks akin to dordite. Magmatic formulae are given.
C. A. S lL B E R R A D .
Pyroxene from Hiva Oa, M arquesas Is., and the form ula of titaniferous augite. T. F. W.
B a r t h (Neues Jahrb. Min., 1931, A, 64, Beil.-Bd., 217—224; Chem. Zentr., 1931, ii, 3095).—The pyrox
ene contained SiO„ 47-11, T i0 2 3-75, A1„03 3-00, F e20 3 3-S4, FeO 12-20, MgO 16-65, CaO 13:54, Na20 0-22, and K 20 0-03%; n a 1-695, n$ 1-701, n v 1-728 (all ±0-003). A. A. E l d r i d g e .
Crystallography of artificial cassiterite. H.
H i m m e l and M. M. P o r t e r (Neues Jahrb. Min., 1931, A , 64, B eil.-B d.,27—33; Chem. Zentr., 1931, ii, 3094).
Cassiterite. H . H i m m e l (Neues Jahrb. Min., 1931, A , 64, Beil.-Bd., 67—70; Chem. Zentr., 1931, ii, 3094).—Vais of n are recorded.
A. A. E l d r i d g e .
O rigin of the silver of K ongsberg from the electrochem ical point of view . L. T r o n s t a d
(Tidsskr. Kjemi Berg., 1932, 12, 15— 18, 28—31).—
Primary Ag may have been formed in three ways,
(a ) by the contact of argentiferous solutions with
certain minerals (pyrites etc.) whereby local currents are generated, (b) by electrolytic pptn. as a result of currents set up by contact of the Ag solutions with minerals which under these conditions give a con
ducting, sparingly-sol. metallic or sub-metallic ppt.
(Beequerel effect), and (c) by “ capillary electric ” pptn. during the passage of Ag solutions through porous rocks. Secondary Ag, especially as wire Ag, may be formed as a result of thermo-electric action, or from effects due to concn. differences. The conclusion is reached that the “ cross rule ” (i.e., that Ag is found only where the lodes are intersected by the fahl- bands) is not of universal application, but that there is a possibility of Ag being pptd. at other points.
H. F. H a r w o o d .
Crystal structure of som e natural and synthetic apatite-lihe substances. S. B. H e n d r i c k s , M. E . J e f f e r s o n , and V. M. M o s l e y (Z. Krist., 1932, 81, 352—369).—Analyses of th e following are given (in this order) (a) fluorapatite from Quebec (cf. A., 1931, 551), (6) chlor-m-apatite from Krageroe, (c) naphtha- extracted bone, (d) (c) steamed for 225 hr. under 40 lb.
pressure, (e) Ca3(P 0 4)2,zH 20 from Na3P 0 4+ C a (N 0 3)2, dried at 50°, (/) hydroxyapatite from Ca3(P 0 4)2 hydrolysed with NH 4 citrate (cf. B., 1931, 199) : CaO 52-40, 52-97, 34-40, 50-96, 47-76, 49-99; MgO 0-46, 0-29, 0-32, 0-67, 0, 0-11; P 20 5 40-30, 40-50, 26*13, 38-47, 40-48, 38-68; F 3-26, 0-17, 0, 0, 0, 0;
Cl 1-16, 4-13, 0, 0, 0, 0 ; C 02 1-51, 0, 3-09, 1-50, 0, 0-12; N a20 + K 20 0, 0-32, 0-54, 0-69, 0-56, 1-01;
SiO„ 3-08, 1-16, 0-09, 0, 0, 0-54; F e20 3 0-60, 0-18, 0-09, 0-13, 0, 0-13; loss at 1000° 1-95, 0-48, 37-61, 8-30, 10-97, 8-56; total (less C 02 and 0 equiv. to F + C l) 100-2,100-8,99-09,99-22,99-77,99-02%. a and c(in A .), d and no. of mols. in unit cell are (6) 9-52, 6-85, 3-25, 2; (c) 9-27, 6-95, 3-25, 2; (e) 9-25, 6-88, 3-01,2; (/) 9-40,6-93,3-08,2; oxyapatite Ca10O(PO4)6 9-38, 6-93, 3-17-3-20, 2; pyromorphite 9-95, 7-31, 7-04, 2 ; mimetite 10-24, 7-43, 7-23, 2; vanadinite 10-31, 7-34, 6-86, 2 (cf. A., 1931, 817). I t is con
cluded that F in fluorapatite can be replaced iso- morphously by C03, OH, S 0 4, S i0 4, O, Cl, Br, or I, thus explaining the occurrence in phosphate rock of minerals such as voelkerite, wilkeite, dahlite, podolite, staffelite, collophanite, etc.
C. A. S lL B E R R A D .
Structure of fibrous sphalerite of the Aachen lead-zinc deposits and the effect of its iron con
tent on the form ation of m inerals. H. E h r e n - b e r g (Neues Jahrb. Min., 1931, A, 64, Beil.-Bd., 397—422; Chem. Zentr., 1931, ii, 3316—3317).
Titaniferous augite from M t. Lobau. P. J.
B e g e r (Neues Jahrb. Min., 1931, A, 64, 71—106;
Chem. Zentr., 1931, ii, 3095).— Optical data are recorded. A. A. E l d r i d g e .
N ew crystals of kipushite. H. B u t t g e n b a c h
(Bull. Acad. roy. Belg., 1932, [v], 18, 43—51).—A detailed description of new crystals of kipushite, a hydrated basic phosphate of Cu and Zn, is given.
C. W. G i b b y .
Radium content of Portuguese m inerals and rocks. G. C o s t a n z o (Rev. Chim. Pura Appl., 1931, [iii], 6, 17—20).—The Ra content of the various Portuguese minerals examined varied from 0-4 to 12-6 g. per 1012 g. The highest figures were obtained for granites, and considerably exceeded those for granites from other regions, whilst tho lowest were obtained for schists. H. F. G i l l b e .
Com position of lithiophilite from Mangualde [Portugal]. A. M. d e J e s u s (Rev. Chim. Pura Appl., 1931, [iii], 6,20—23).—The mineral has a com
position approx. corresponding with MO,2M'O,P205, where M is Mg, Ca, Li2, or Na2, and M' is Mn or Fe.
I t contains Li20 8-04%, N a20 1-33%, CaO+MgO
2-16%. “ H. F. G i l l b e .
R elationships of the granites to the rhyolites in S.E . M issouri. W. A. T a a r (Science, 1932, 75, 265).—Evidence has accumulated showing that tie granites in S.E. Missouri are younger than the rhyo
lites and have been injected into them.
L. S. T h e o b a l d .
Differentiation and sequence [of the e r u p t i v e
rocks] in the Bohem ian M idland Mountains, H .
I C n o r r (Tsch. Min. Petr. Mitt., 1932, 42, 318—370).
— 104 analyses of igneous rocks of Tertiary age from northern Bohemia are tabulated, including 14 new analyses of trachyte, sodalite-syenite, essexite, and nepheline-basalt. The differentiation of the several rock types from an original basaltic-basanitic m a g m a
is traced. L. J. S p e n c e b ,
Gold and bism uth in the spathic iron veins o!
Siegerland. J. M. H u t t e n h a i n (Tsch. Min. Petr.
Mitt., 1932, 42, 285—317).—The FeC 03 veins of the Siegen district, on the borders of Westphalia and Rheinland, contain gold of two generations. The earlier is contained in an invisible form, perhaps as sulphide, in pyrite (6-23 g. per ton). The later generation occurs as minute particles of free Au in association with Bi minerals (Bi, Bi2S3, klaprothite, etc.). They belong to different phases of the hydro- thermal processes (arising from a hidden mass of igneous rock) which deposited the material in the
veins. L. J. S p e n c e r .
Spectroscopic investigation of Brazilian tourmaline. G. 0 . W i l d (Zentr. Min., Geol., Palaont., 1931, 327—330; Cliem. Zentr., 1931, ii, 2589).—The red and the rose-coloured tourmaline from the mines near the bridge between Arassuahy and Itinga, and the green rocks of the Barra de Selinas, Minas Geraes, have been investigated with a quartz spectrograph and C arc. Ga, Sn, Na, Ca, and Li are present in the red rocks, but Mg is absent. The green tourmaline showed the principal Fe lines, and strong lines due to Mn, Li, Ca, and Mg, but not Ga. A rose- coloured rock showed no Mg lines. L. S. T h e o b a l d .
Occurrence of telluride m inerals at Kalgoorlie.
p . L. S t i l l w e l l (Proc. Austral. Inst. Min.. Met., 1931, [ii], No. 84, 115— 190).—A description of the following minerals and of their occurrence is given, together with their associated o res: PbTe, IigTe, NiTe2, a-CuTe,2/Cu2Te, Ag2Te, Au2Te,3Ag2Te, AuAgTe4, (AuAg)Te2, Au(Ag)Te2, (PbA u)(ST eSb)^
• C. W. G i b b y . *
Constitutional formulae of spinels. H. R h e i n - b o ld t (Rec. trav. chim., 1932, 51, 356—360).—A
lecture. E. S. H e d g e s .
Quantitative m ineralogical com position of Tertiary sands in the subsoil of H am burg and its neighbourhood. H. M u l l e r (Zentr. Min., 1931, 278—296; Chem. Zentr., 1931, ii, 2590).—The follow
ing sedimentary types have been distinguished (i) pyrite-ilmenite-corundum, (ii) rutile-ilmenite-corun- dum, (in) cyanite-ilmenite-corundum, and (iv) am- phibole-ilmenite-corundum. These types agree with the sedimentation cycle revealed bythefelspar contents of the individual horizons. L. S. T h e o b a l d .
Nature of clay. F. H. N o r t o n and F. B. H o d g - d o n (J. Amer. Ceram. Soc., 1932, 15, 191—205).—
The particle spacing (calc, from the bulk-d) of a no.
of plastic and non-plastic materials was determined for varying conditions of pressure and H aO content.
All materials at the low pressures (SO kg. per sq.
cm.) have a crit. H 20 content (pores half-filled) below which addition of H 20 causes little change in v ol., but above which the particles re-orient themselves into a closer packing with a more or less sudden decrease in vol. A saturation point is reached at higher H20 contents. The non-plastic materials are distinguished only by the absence of drying shrinkage.
A t high pressures (up to 800 kg. per sq. cm .) the particle spacing is proportional to the logarithm of the pres
sure and a marked elastic return is found on releasing the pressure. The min. particle spacing at high pressures occurs at the saturated point, and beyond this point additional H ,0 forms thick films around the particles of such stability that they are not in
fluenced by pressures of 800 kg. per sq. cm. and the drying shrinkage is also unaffected. Bentonite gave results which indicate close packing of plate-like particles. The plasticity of clays is due to the adsorption on the surface of the particles of a film of H20 about 3 X 10~5 cm. thick which provides both the cohesion and lubrication. J. A. S u g d e n .
Genesis of coals. II—TV. E. B e r l and A.
S c h m i d t . —See B., 1932, 245.
Soil charting in the U .S .A . H. K e l l e r (Z.
Pflanz. Diing., 1932, 24, A, 38—44).—The val. of American methods is discussed. A. G. P o l l a r d .