Recent foraminifera in glaciomarine sediments from three arctic fjords of Novaja Zemlja and Svalbard S . A . KORSUN, I. A . POGODINA, S. L. FORMAN AND D. J . LUBINSKI Korsun. S . A,, Pogodina, 1. A . , Forman. S . L. & Lubinski, D. J . 1995: Recent foraminifera in glaciomarine sediments from three arctic fjords of Novaja Zemlja and Svalbard. Polar Research, 14(1), 15-31. Foraminifera were examined in recent (< 100 years) fine-grained glaciomarine muds from surface sediments and cores from Nordensheld Bay, Novaja Zemlja. and Hornsund and Bellsund, Spitsbergen. This study presents the first data o n modern foraminifera distribution for fjord environments in Novaja Zemlja, Russia. The data are interpreted with reference to the distribution of foraminiferal near Svalbard and the Barents Sea. In Nordensheld Bay, live and dead Noniortellino labradorica and Islaniiiella norcr0sr.i are most abundant in the outer fjord. Cassidulina reniforme and Allogromiina spp, dominate in the middle and inner fjord. The dominant species are dissimilar to species occurring in other areas of the Barents Sea region, with the exception of Svalbard fjords. The number of live foraminifera (24 to 122 tests/lO cm') in outer and middle Nordensheld Bay corresponds with values known from the open Barents Sea. However. the biomass (0.03 mg/lO cm') is two orders of magnitude less due to smaller foraminiferal test size, which in glaciomarine sediments reflects the absence of larger species, paucity of large specimens. and high occurrence of juvenile foraminifera. The smaller size indicates an opportunistic response to environmental stress due to glacier proximity. The presence of Qubiquelocitlina stalkeri is diagnostic o f glaciomarine environments in fjords of Novaja Zemlja and Svalbard. S. A . Korsun and 1. A . Pogodina, Murmansk marine Biological Institute. 17 Vladimirskaya St., Murmansk 180023, Russia; S . L . Forman, B y d Polar Research Center and Department of Geological Sciences, The Ohio State University, Columbus. Ohio 43210-1002, U . S . A . ; D . J. Lubinski, Institute for Arctic and Alpine Research and Department of Geological Sciences, University of Colorado. Boulder. Colorado 80309-0450, U.S.A. (Direct correspondence to S . L . Forman). n ''*PoLAR\NS''' Introduction Studies of foraminifera from recent glaciomarine sediments provide insights into the environmental significance of taxa and potentially improved paleoenvironmental inferences for fossil faunas. A number of studies have examined benthic fora- minifera from Svalbard fjords (Goes 1892, 1894; Kiar 1899; Feyling-Hanssen 1964; Nagy 1965; Rouvillois 1966; Luczkowska 1975; ElverhJ et al. 1980; Kirienko 1984; Hansen & Knudsen 1992; Hald & Korsun unpublished). In contrast, for- aminiferal faunas from the subpolar fjords of Novaja Zemlja have not been investigated except for a study of reworked fauna from sea ice and icebergs (Potekhina et al. 1992). Glacier proximal foraminiferal assemblages in Svalbard fjords are typically dominated by the calcareous species Cassidulina reniforme and/or Elphidium clavatum and have low values for fau- nal diversity, planktic/benthic ratio, and number of tests (Nagy 1965; Luczkowska 1975; Elverhd et al. 1980; Kirienko 1984; Hansen & Knudsen 1992; Hald & Korsun unpublished). These assem- blages are common in late Pleistocene records from the southwestern Barents Sea and Norweg- ian shelf and are assumed to indicate glacier prox- imity. The C. reniforrne-E. clauatum assemblages are replaced upcore, near the Pleistocene/Hol- ocene transition, by a variety of other assemblages which indicate full marine conditions and pen- etration of warm Atlantic Water into the area (e.g. Bstby & Nagy 1982; Vorren et al. 1984; Hald et al. 1989). In contrast, foraminiferal assemblages from Holocene marine-muds in the northern Barents Sea are often similar to faunas from glacio-marine sediments of Svalbard fjords, with co-dominance of C. reniforme and E . clav- atum, and low faunal diversity, planktic/benthic ratio, and number of tests (Sakharova & Korsun 1989; Spiridonov et al. 1992; Korsun et al. 1994). Our analysis of eight modern samples from Nordensheld Bay provide new data on the dis- tribution of foraminifera in Novaja Zemlja fjords. These data comprise a basis for comparing and possibly extending established relations between 16 S . A . Korsun et al. modern foraminifera in a Novaja Zemlja fjord with other areas in the Barents Sea region. For- aminiferal test size and minor species composition Hydrographic and sediment settings Hornsund and Bellsund, Svalbard for glaciomarine sediments from Nordensheld Bay, Novaja Zemlja, and Hornsund and Bell- sund. Spitsbergen, were analysed to further evalu- ate the differences between foraminifera1 faunas of the open northern Barents Sea and glaciated fjord environments o n the adjacent archipelagos. T h e West Spitsbergen Current, a northern branch of the Gulf Stream, transports relatively warm and saline (T > 1°C and S = 34.7%0) Atlantic Water along the western coast of Svalbard (Fig. 1). This water penetrates often at depth into fjords along the western coast of Spitsbergen, 80" N 780 76" ,\ 70" F i g . I . l'hc Bdrents Sea region' Atlantic ( 1 ) . Arctic ( 2 ) . and Coastal ( 3 ) surface currents (Tantsiura 1Y73. simplified): convergence zone ( 4 ) and mining zone ( 5 ) of the Polar Front ( T a n t m r a 1Y7i): Boreal/.Arctic zoogeographic boundary of benthic foraminifcra ( h ) ( D i p \ 1971)) Recent foraminifera- in glaciomarine sediments 17 including Hornsund and Bellsund. During the winter, sea ice covers the fjord head and rarely extends to the open sea (Vinje & Kvambekk 1991). Associated with sea ice formation at the fjord head is descending cold and saline (T < 0°C and S > 35%0) water. The summer melting of adjacent glaciers is a source of a low salinity (>20%0) surface layer in the upper 5 to 15 m (Norman 1987; Weslawski et al. 1991). The sedimentation rate decreases exponentially from many glacier termini o n western Spitsbergen (Elverhcji et al. 1983; Boulton 1990). All three sampling sites are situated in the vicinity of calving glaciers (Figs 2, 3 and 4) and within an area of meltwater discharge (August 1990). The con- centration of suspended sediment at sampling site 15" E 20" D 1 Fig. 2 . Spitsbergen and location of study sites in Bellsund and Hornsund. Ho-3 in Hornsund, Spitsbergen, ca. 0.5 km from the Hansbreen outlet, was about 300 mg/l in the surface water in July 1983 (Gorlich et al. 1987). Sedimentation rate in the glacier-proximal zone usually does not exceed 350 mm/yr within 0.3 km from the Hansbreen outlet and is less that 1 mm/ yr in the glacier-distal zone, approximately > 5 km from the glacier termini in Hornsund (Gor- lich et al. 1987). Nordensheld Bay, Novaja Zemlja There is little information on water masses in the Nordensheld Bay area, Novaja Zemlja ("Norden- sheld" is a double transliteration, Norwegian from Russian to Latin, of G . Nordenskjdd name). The Barents Sea shelf in the vicinity of Nordensheld Bay is occupied by cold Arctic Water (T = - 1°C and S = 34.8%0). Nordensheld Bay and the adjac- ent shelf are usually covered by sea ice for at least six months of the year. (Murmansk Hydro- meteorological Survey 1988; Vinje & Kvambekk 1991). The only summer hydrographic profile is at site 874, which shows a lower salinity surface layer (0-10 m; 31.3-31.5%0) and normal marine values for bottom waters (34.8%0) (Chinarina 1992). At the head of Nordensheld Bay is the large calving Nordensheld Glacier (Fig 6). An extensive meltwater system emanating from the glacier ter- minus delivers turbid fresh water to the fjord. Although the exact sediment concentration is not known for the sampling period, an earlier investigation during August/September 1984 measured a water column suspended sediment (fine silty-clay) concentration of 88 mg/l ca. 10 km from the glacier terminus (Aksyonov 1987). Gla- ciomarine sediments in the upper part of the fjord are characterised by 1 to 10 cm thick laminae of light gray silty-clay (Tarasov et al. 1993). Material and methods In Nordensheld Bay, northern Novaja Zemlja, four grab samples (896, 874, 894, and 895) and two gravity cores (894 and 895) were retrieved by the R/V DALNIE ZELENTSY in late August and early September 1991 and four additional box-core samples (68/31, 68/3, 68/32 and 68/33) were col- lected in August 1991. The distal samples (68/31, 68/3,68/32, and 896) have diagenetic colour strati- fication, characterised by a 2-cm-thick light-olive 18 S. A . Korsun et al. I 14'00' 1 4 ' 3 0 ' Bellsund oxidised surface-layer. overlying light-gray mud. Sediments. more proximal to the glacier (samples 874.894.68/33, and 895). d o not have an oxidised layer but consist of light-gray mud. Both cores penetrated uniform laminated light-gray fine- grained glaciomarine sediments (Table 1: Figs. 5 and 6 ) . Three gravity cores (Bel-1, Ho-2. Ho-3) from Bellsund and Hornsund were obtained by the w'v POMOR in August 1990 (Fig. 2 and 3). T h e recovered glaciomarine sediment is light gray with a low sand and gravel content (0.5-3%). T h e individual sediment cores were sampled at either 5. 10, or 20 cm intervals. T h e thickness of Fig. 3. Location of core Bel-1 in Bellsund. proximity to Recherchebreen Recherchehreen the sampled interval is 5 cm. The samples were dried, weighed, sieved (>0.063 mm), and floated with carbon tetrachloride to isolate foraminifera1 tests. T h e number of foraminifera counted for each sample ranges from 100 to 350 specimens. T h e greatest diameters of C. renifornie tests in core t o p samples (0-5 cm) of the fjord cores 894, 895, and Ho-2 and the previously studied cores 671.666, and 396 from the open Barents Sea were measured to compare the mean test-size of an individual species in glaciomarine and marine sediments. C. reniforrne were chosen for the analysis because of its abundance in both the fjord and Barents Sea samples. T h e greatest diameter 15" 4 0 ' 16' 00' 16'20' Fig. 4. Location of core Ho-2 in Hornsund. Recent foraminifera in glaciomarine sediments 19 Table 1. Station list Sediment Surface Station Collected Date Depth (m) Sediment General Location Latitude N Longitude E 6813 68/31 68/32 68/33 874 894 895 896 Bel-1 Ho-2 Ho-3 653 646 396 666 67 I Box Core Box Core Box Core Box Core Grab Grab Grab & Core Grab & Core Core Core Core Grab Grab Core Core Core 8 / 19/92 8/30/92 8130192 8/30/92 8/18/91 8/29/91 8/29/91 8/30/91 Samples investigated in this study Nordensheld Bay, 139 mud Novaja Zemlja 165 mud 120 mud - 45 mud 76 mud 31 mud 49 mud - 149 mud ,, - I, I , ,, ,, - ,I I, - !I ,I - I, ,I I, , I - ,I Belsund, W 40 mud Spitsbergen Hornsund. W 60 mud Spitsbergen 30 mud It - ,I 75" 28.0' 56" 44.2' 75" 33.3' 56" 21.1' 75" 28.5' 57" 10.0' 75" 21.5' 57" 35.8' 75" 22.0' 51" 29.0' 75" 19.7' 57" 30.2' 75" 20.0' 57" 45.0' 75" 24.7, 570 06.0, 77" 26.0' 14" 40.0' 77" 04.0' 16" 17.0' 77" 04.0' 15" 38.0' Previously studied samples used for comparison 10/15/87 290 mud NE Barents Sea 10/12/87 200 sandy mud " ~ " 130 mud South off Svalbard 380 mud - 315 mud, pebbles " - " I, I, 77" 37.0' 55" 57.0' 75" 58.0' 48" 13.0' 76" 58.6' 28" 12.1' 7.5" 55.0' 15" 54.0' 76" 10.0' 16" 21.0' 52O 56O 60' 64' 6 8 O 770 76O 7 50 740 730 72' 1 Fig. 5 . Locationof Nordensheld Bay onNovaya Zemlja, Russia. was measured for a minimum of 20 tests for each sample. The location of the previously studied cores is shown in Fig. 1. Foraminifera from eight modern samples (20- 100 cm3 of the upper 1 cm) were preserved with 80% ethanol ( 5 : 1 by volume), assuming dilution to 70% due to the sediment water content. The samples were stained for one day with Rose Ben- gal (1 g/l) and then wet sieved through 0.063 mm sieve. Four samples from box cores (68/31, 68/3, 68/32, and 68/33) were dried and floated as above. Live (stained) and dead (unstained) fora- minifera were counted. The other four samples (896,874,894, and 895) were wet sieved to isolate the >1.0, 1 . 0 4 . 5 , 0.5-0.25, 0.25-0.100 and 0.100-0.063 mm fractions of foraminifera1 tests for a size class analysis and biomass measure- ments. Biomass is evaluated by a cytoplasmic volume calculation for four different size fractions. In each fraction a biomass was estimated by the following formula: W = 0.1 x S3 x n. where W = biomass, n = number of live fora- minifera, and S = mean diameter of foraminifera 20 S. A . Korsun et al. Fig. 6. Location of sampling sites in Nordensheld Bay, Novaya Zemlja, Russia. (Korsun 1991). Means of the diameter (S value) for the following size fractions are: 0.0794 mm Modern foraminifera in Nordensheld Bay, Nooaja Zendja (0.063-0. I mm fraction). 0.158 mm (0.1-0.25 mm fraction), 0.354 mm (0.25-0.5 mm fraction). and 0.707 mm (0.5-1.0 mm fraction). Two previously studied grab samples from northeastern Barents Sea (646 and 653) a r e used to illustrate differences in Nordensheld Bav. T h e number of tests counted for each modern sample ranged from 35 to 416 specimens for total fauna from 17 to 148 specimens for live fora- minifera. Total fauna is the sum of live and dead foraminifera in modern samples. W e use the term ‘fossil’ for tests from the core samples. except for the core tops which are composed of live and dead foraminifera (total fauna). Results A total of 59 foraminiferal taxa are identified for samples from Novaja Zemlja and Svalbard (Table 2 ) . Most of the species are characteristic of Arctic foraminiferal faunas of the Barents Sea region (Digas 1970). Foraminifera1 fauna includes organic-walled Allogromiina spp., 23 arenaceous and 36 calcareous taxa. The only recent siliceous foraminifera known for the Barents Sea. S. groen- landica, was absent in o u r samples of glaciomarine sediments. Modern foraminifera were studied in eight surface sediment samples from Nordensheld Bay (Fig. 6 ; Tables 3 and 4). Live and dead N . labradorica and I . norcrossi a r e abundant in t h e outer fjord (sites 68/31, 6813, and 68/32). C . renifornie and Allogromiina spp. dominate in t h e middle and inner fjord. Q. sralkeri occurs only in the middle and inner fjord. S. biformis and E . clavatum show unclear distribution patterns (Fig. 7). T h e number of dead foraminifera comprises 152 t o 170 tests/10cm3 in the inner fjord and decreases consistently toward the glacier from 46 t o 1.5 tests/10cm3. T h e number of live fora- minifera ranges from 24 to 122 tests/lO cm3 in the outer and middle fjord and drops to between 3 and 6 tests/l0 cm3 in the two samples closest t o the glacier terminus. Calcareous faunas make u p 68 to 97% of live foraminifera in the outer fjord. In the middle and inner fjord, the percentage decreases from 77 to 8% toward the glacier, reflecting the increasing significance of Allo- gromiina spp. T h e percentages of dead calcareous foraminifera varies from 46 to 100% (Fig. 8) and does not show consistent trends with position in bay. T h e total benthic fauna includes 12 to 35% of live specimens in the outer fjord; in the middle a n d inner fjord, the value exceeds 50%. T h e Recent foraminifera in glaciomarine sediments 21 Table 2. List of identified foraminifera1 taxa Adercotryma glomerata (Brady, 1878) Allogromiina Alueolophragmium crassimargo (Norman, 1892) Ammodiscus sp. Ammotium cassis (Parker, 1870) Asfrononion gallowayi Loeblich & Tappan. 1953 Boliuina pseudopunctatn Hoglund, 1947 Bolicrina sp. Buccella frigida (Cushman, 1922) Cassidulina reniforme Nsrvang. 1945 Cibicides lobanclus (Walker & Jacob, 1798) Cribrostomoides jeffreysi (Williamson. 1858) Denfalina baggi Galloway & Wissler, 1927 Eggerella advena Cushman, 1922 Elphidiella arctica (Parker & Jones, 1864) Elphidium albiumbilicatum (Weiss, 1954) Elphidium clavatum Cushman. 1930 Elphidium subarcficum Cushman, 1944 Episfominella sp Fissurina marginata (Montagu, 1803) Fissurina sp. Gavelinupsis praegeri (Heron-Allen & Earland. 1913) Globobulimina turgida (Bailey, 1851) Hippocrepinella alba Heron-Allen & Earland, 1932 Hyperammina subnodosa Brady, 1884 Islandiella helenae Feyling-Hanssen & Buzas. 1976 Islandiella norcrossi (Cushman, 1933) Lagena gracillima (Seguenza, 1862) Lagena semilineata Wright, 1886 Melon& barleeanus (Williamson, 1858) Miliolinella pyriformis Gudina, 1969 Miliolinella sp. Neogloboquadrina puchyderma (Ehrenberg, 1861) Nonionella auricula Heron-Allen & Earland. 1930 Nunionella turgida (Williamson, 1858) Nonionellina labradorica (Dawson. 1960) PateNina corrrcgata Williamson. 1858 Pelosinu variabilis Brady, 1879 Polymorphinidae Proelphidirtm niveum (Lafrenz, 1963) Profelphidiitm orbiculare (Brady, 1881) Proteeoriina sp. Psammosphuera sp.2 Quinqueloculina stalkeri Loeblich & Tappan. 1953 Recurvoides rurbinatus (Brady, 1881) Reophax arctica Brady, 1881 Reophax atlantica (Cushman, 1944) Reophax scorpiurus Montfort, 1808 Reophax scotfii Chaster, 1892 Robertina arctica d o r b i g n y , 1846 Rosalina spp. Rotaliammina ochracea (Williamson, 1858) Spiroplecramminn biformis (Parker & Jones, 1865) Stairzfortlria loeblichi (Feyling-Hanssen. 1954) Stainforthta schreibersiana Czjzek, 1848 Textularia earlandi Phleger, 1952 Terttularia rorquata F. Parker. 1952 Trifarina puens (Todd, 1947) Trochammina nana (Brady, 1881) Trochamminella atlanrica F. Parker. 1952 Trochamminella brrllara Hoglund, 1947 Trochamminella sp. number of live species per sample decreases gradually toward the glacier. The number of dead species is 22 to 23 in the outer fjord and 2 to 8 in the middle and inner fjord. (Table 4; Fig. 8). Foraminifera1 biomass is evaluated for four samples (896,874,894, and 895) and ranges from 0.001 to 0.030 mg/lO cm3. The lowest value is observed in the sample closest to the glacier ter- minus (Table 4). An analysis of size spectra in these four samples reveals that neither live nor dead foraminifera occur in sieve fractions greater than 0.25 mm. Recent foraminifera in cores f r o m Nordensheld Bay, Novaja Zernlja, and Hornsund and Bellsund, Svalbard We infer that the sampled sediments in close proximity to present glacier margins were deposited in the last few hundred years. Sedi- mentation rates near core site Ho-3, Hornsund, are approximately 350 mm/yr (Gorlich et al. 1987) and thus, the 60-cm-length of sampled sedi- ments probably spans < 10 years. The proximal core site 895 in Nordensheld Bay is located behind the end moraines of a presumed Little Ice Age advance of Nordensheld glacier (Fig. 6; Forman unpubl. data). We speculate that the sediments at site 895 were deposited after the glacier retreat ca. 1900 A . D . In the upper part of Nordensheld Bay, individual sediment laminae are from 1 to lOcm thick. Tarasov et al. (1993) assumed that the laminations were seasonal, and thus the two studied cores may span decades or centuries. We estimate that the sedimentation rate for the cores studied is two to three orders of magnitude higher than in the central Barents Sea where the appar- ent Holocene sedimentation rate is approximately 0.1 mm/yr (Gataullin et al. 1993). The downcore distribution (Figs. 9 and 10) illustrates the general continuity and short term variations of taxa in these sediments. The dominant species in the five studied cores are C. reniforme and E . clavatum (Figs. 9 and 22 S. A . Korsun et al. Table 3 Number of live and dead foraminifera per 10cm' in Nordensheld Bay. Novaja Zemlja Station 68/31 68:3 68/32 896 874 894 68/33 895 Live L L L L L L L L Dead D D D D D D D D Allogromiina spp. Hippocrepirtella alba Psuinrnospliaeru sp.2 Proreoninu \ p . Pelosina ouriuhilis Hyperamrriiriu subnodosa Ammodurw s p . R e o p h a r aflunticu Reopliax S L ( ~ r p i u r ~ Reop1ia.x urrticu Reophux scorrii Ammoriuni 1us1.1 A l v e o l o p h r u g m i u m crassintargo Cribrosromoides jejjreys I Adercorrwnu glomerara Recuriwides rurbinuricc Trochuniinrnella hullaru Irochammiita nuna .Spiroplecrurni~iirta hiformi\ €ggrrrlla urloenu C'orniupira , p . ~ i i i r i q i i e l o ~ ~ i r / i ~ i u srulkerr Miliolinellu sp Qhicider Ioburulro Kosulina s p . Buctelh frrgidu .Voniuriellinu lubrudoriro .4srronoiirori gullonq I Proteiphrdiiirn orhicirlure E l p h i d i i r i n riihar~~iicurn Elphiiliuni ~ ~ I r i t ~ u r i i ~ n Cu.5 ~ i d u l i n u rrrii jo rinr 1.0 1.0 2.5 2.5 1.5 1.5 i n 0 52.0 26.5 3.0 2 0 6 0 10.5 0 4 2.0 1 .0 0.3 0 5 0.2 18.0 1.5 0.5 0 . 5 0.5 3.5 1.0 1.0 3.0 1.5 7.0 0.5 0.5 4.0 4.0 2.0 6.5 33.5 0.5 0 5 2.0 0.5 1 .o 0.5 2 . 5 8.5 1 . 0 15.5 1 .o 1 0 6.0 0 . 5 10.5 5 . 5 1 .o 0 5 2 0 2 5 0.5 1 0 2 5 4 . 5 0.5 2.0 2.5 2.5 6.0 10 0 0.7 3.0 0 5 14.0 6 . 0 2.5 0.5 7.0 2 . 0 6.5 2.0 0.1 2.0 0.5 0.3 1 .0 4.0 0.3 0.3 0.5 2 . 5 2 . 0 9.0 1 0 10 5 6.0 2 1 . 5 7 5 2 1 ( 1 I4 0 1 5 10.5 3.0 11 0 0.5 0 . 5 J.5 2.0 0.5 1 5 1 .u 78 5 I4 0 6 5 7 5 1 .0 34.5 29 0 6.5 5 0 2.0 6.5 1.0 2 . 0 1 . 5 0.3 0.4 28 0 8.0 1 . 5 2.0 0.5 50.0 52 0 6.0 0.7 0. I 0 5 6.5 9 0 Recent foraminifera in glaciomarine sediments 23 Table 3 . Continued ~ ~~ Station 68/31 6813 68/32 896 874 894 68/33 S95 Live L L L L L L L L Dead D D D D D D D D Islaridiella riorcrossi + Islandiella helenae 11.0 13.5 Bolivina pseudopicnctata 1.5 10.0 19.5 31.5 0.5 Trifarina pueris 0.5 0.5 0.5 1.0 3.0 Stainforrli ia Ioeblich i 0.5 2.5 Globobulimina ticrgida 0.5 Dentalina baggi 0.5 Stairiforrhia schreibersiana Robertina arctica 0.5 0.5 Lageria sernilinema 0.5 6.0 1.5 0.1 10). T h e arenaceous foraminiferan S. biformis and the calcareous foraminifera Q. stalkeri, C. lobatulus. Buccella frigida, and N . labradorica in some intervals comprise > 15% of the fauna. T h e ambiguous morphology ( 2 o r 3 chambers) of many small-sized (ca. 0.063 mm) juvenile tests preclude identification to genus. These smaller tests com- pose up to SO% of the fauna in certain levels and Table 4. Faunal and environmental characteristics of the foraminifera1 distribution in Nordensheld Bay. Novaja Zemlja (N/A = none analysed) Station 68/31 6813 68/32 896 874 894 68/33 895 Live L L L L L L L L Dead D D D D D D D D Benthics/IO cm3 9% Calcarcous foraminifera Calc/lO cmj Live Calc./Total Calc. Benthics Counted No. of species, All No. of species, Calcareous % Live Biomass, mg/lO cm3 23.5 68 16.0 170 0 46 78 0 0.17 3’0 23 10 47 13 5 12 N i A 47.0 93 43.5 151.5 81 123.0 0.26 264 22 11 72 10 7 24 N/A 87.5 97 84.5 165.5 91 150.5 0.36 268 22 12 148 11 8 35 N/A Planktics Counted (Neogloboquadrina pachyderma sin) Distance from glacier. km 48 36 25 % sediment fraction >0.063 mm 5.4 7.4 4.5 1 Sea depth. m 165 139 120 94.0 77 72.0 46.0 70 32.0 0.69 23 5 3 47 9 5 67 0.021 24 149 2.5 122.0 52 64.0 10.0 100 10.0 0.86 5 2 2 61 5 3 92 0.030 12 76 0.9 73.5 24 18.0 13.5 78 10.5 0.63 27 8 5 147 10 6 84 0.029 10 31 0.3 5.7 6.0 83 5.0 0.29 18 6 5 35 2.0 17 5 3 49 N/A 7 45 0.3 2.6 8 0.2 1.5 67 I .I) 0.17 15 5 3 26 4 2 63 0.001 3 49 0.1 24 S. A . Korsun et al. _ _ _ _ _ _ _ _ _ _ _ _ - - _ _ - - - - Cassidubna renilorme . . . . . . . . . . . . . . . . . . . . R g 7 The distribution of live dead benthic foraminifera (tests/lO cm3) in Nordensheld Bay, Novala Zemlja (collected i n . . . . . . . . . . . . . . . . . . . . _ _ _ _ _ _ _ _ _ _ _ _ - - - _ - - - - . . . . . . . . . . . . . . . . . . . . 68/31 68/3 68/32 896 874 894 68/33 895 late August and early STATION are referred t o as ‘Varia uv.’ (Figs. 9 and 10). T h e number of benthic species/sample and number of tests/100 g d o not exhibit consistent downcore trends. Planktic foraminifera a r e rare in fjord sediments. reflecting the limited number of trans- ported tests. The abundance of foraminifera appears to increase with distance from the main outlet glacier i n fjords o n Spitsbergen and Novaja Zemlja. Cores Ho-3 and Be-1 from Hornsund and Bell- sund collected within 0.5 km from the outlet gla- cier terminus at water depths of 30 m and 40 m , respectively. have a foraminifera abundance of Septeniher 1990 and 1991). < 100 test/100 g of sediment (Fig. 10). In contrast, core Ho-2. collected at ca. 2 km from the main outlet glacier at a water depth of 6 0 m has an abundance exceeding 200 tests/100 g (Fig. 10). A similar trend in foraminifera abundance is also recognised for glacier proximal and distal sites in Nordensheld Bay, Novaja Zemlja (Fig. 10). Cassidulina reniforme test size Initial observations indicated that tests of an indi- vidual species from fjord environments a r e smaller than tests from the Barents Sea. A series Recent foraminifera in glaciomarine sediments 25 150 100 50 0 - NO. of species per sample Oxidized surficial sediment layer +----- present - absent __* Fig. 8. Selected faunal and environmental characteristics of the foraminifera1 distribution in Nordensheld Bay, Novaja Zemlja (collected in late - - 8,0 % sediment fraction >0.063 mm August and early 68/31 6813 September 1991 and 1992). of comparative measurements of C. reniforme tests from fjord and Barents Sea environments were undertaken to quantify these observations (Table 5 ) . Intersample differences in mean test size for glaciomarine and marine sediments are insignificant (Fig. 11). In contrast, the difference between the mean of the greatest C. reniforme diameter from glaciomarine sediments and the mean value for marine sediments is significant at the highest standard confidence level, tfact = 6.20 > to,ool = 3.29. Tests are considerably larger in the Barents Sea, averaging at least 40 pm larger diameters than fjord specimens (Fig. 11). There are distinctive differences between Nor- densheld Bay foraminifera assemblages from the open Barents Sea and the coastal zone of Kola Peninsula, Svalbard, and Franz Josef Land. These near-shore areas are situated to the north of the Boreal-Arctic zoogeographic boundary of fora- minifera (Fig. 1; Digas 1970). In comparison with Novaja Zemlja. the Svalbard fjords are similar in terms of presence of meltwater plums in the vicin- 26 S. A . Korsun et al. 895 ( 4 5 m) ! 8 9 4 ( 3 1 m) 1 -I+- = = - = - - - - - 1 - - --- - - ore No (Sea depth) listancs from glacier Weight % of sediment ~ fraction >O 063 mm Sample, depth in core (cm) Allogromiina spp Hrppocreprnella alba Reophax arctrca Trocharnrninella etlantrca Rotaliarnrnina ochracee Sprropleclarnmina brforrnrs Eggerella advena Ournqueloculina slalkerr Mrlrolmella pyrrformrs Patellma corrugata Cibicrdes lobatulus Rosalrna spp Gavelrnopsrs praegerr Buccella frigida Eprstornrnella sp Nonronella auricula Nonionellrna tabradorica Melonis barleeanus Astrononion gallowayi Protelphtdrum nrveum Elphidturn albrumbrlrcaturn Elphrdiurn subarcticurn Protelphrdrum orbiculare Elphrdium clavaturn Cassrdulrna renrforme lslandislla helenae lslandrella norcrossi Trrfarrna fluens Starnforfhia loeblrchr Stainforthfa schrerbersran. Bolivrna pseudopunctale Polymorphinidae spp Lagena gracrllrrna Fissurrna margrnata Varia uv 2 N pachyderma dex .A - N pachyderrna sin -- A _- - -0 ~ 0 Number of benthic N foraminifera per lOOg ) ;;O 0 of dry sediment - ,n Number of species ity of the subpolar glaciers. T h e Kola Peninsula does not have tidewater glaciers or any glaciers in vicinity of the coastline. Although Franz Josef Land is almost entirely covered by ice caps. these polar glaciers produce rare melt water plums. In Nordensheld Bay. N . labradorica and I . norcrossi are the most abundant species in the outer fjord (68/31.68/3. and 68/32). C. reniforme and Allogromiina spp. dominate foraminiferal fauna closer to Nordensheld glacier (Fig. 7). These taxa generally comprise a low percentage of the total foraminiferal fauna in the open Bar- ents Sea (Digas 1970: Korsun et al. 1994), the coastal zone of the Kola Peninsula (Korsun 1986. 1992) and Franz Josef Land (Basov 1961; Lukina 1Y77). Fig. 9. Foraminifera1 distribution i n cores 895 and 894 from Nordensheld Bay, Navaja Zemlja. T h e r e are broad similarities in the distribution of foraminifera in Nordensheld Bay and the fjords of Svalbard. N . labradorica and C. reniforme are two of six principal species identified from six fjords o n western and northern Spitsbergen (Hald & Korsun, unpubl.). C. reniforme appears to inhabit environments closer t o the fjord head while N . labradorica increases in abundance out- fjord. C. renifornte is an opportunistic species and often dominates foraminiferal assemblages in htressed/unstable environments proximal to gla- cier discharge (e.g. Osterman & Nelson 1989). W e assume that t h e substitution of N . labradorica and I . norcrossi by C. reniforme in Nordensheld Bay reflects increasing ecological instability toward the glacier. Recent foraminifera in glncioninrine sedinients 27 2 - 0 0 N u m b e r o f b e n t h i c f o r a m i n i f e r a per 1 0 0 g . of dry s e d i m e n t 0 2 - ul 0 20 7 10 Number of s p e c i e s I 2 r 0 I s V e Fig. 10. Foraminifera1 distribution in cores Be-1, Ho-3, and Ho-2 from Bellsund and Hornsund, Svalbard. C o r e N o ( S e a d e p t h ) D i s t a n c e f r o m g l a c i e r - N W e i g h t YO of s e d i m e n t f r a c t i o n >0.063 mm S a m p l e . d e p t h in c o r e ( c m Reophax scottii Adercotryma glomerata Trochamminella sp. Spiroplectammina biformis Eggerella advane Ouin ueloculine stalkeri Pate&na corrugate Cibicidas lobatulus Rosalina app Buccella lrigida Nonionelline tabradorica Melonis barleeanus Astrononion gallowayi Elphidium subarcticom Elphidium clavatum Cassidulina reniforrne lslandiella helenae Sleinlorlhia leoblichi Bolivina sp. Polymorphinldaa spp. Lagena gracillima Fissurina sp. Varia uv. N. pachyderm8 dex. N. pachyderm8 sin. C . reniforrne and another characteristic glacier- N u m b e r of live foraminifera and biomass in proximal cakerous species, E. clavatum, co- Nordensheld Bay dominate In outer and middle Nordensheld Bay (st, 68/31 densheld (Fig. 9, and cal- through 894), the glaciomarine mud contains 24 in the two Nor- careous assemblages in grab samples 894 and 895 distribution of E . clavatum in Nordensheld Bay remains unclear. to 122 live specimens/l0 cm3 (Fig, 8). This is Barents Sea where values mainly range from 25 to 200 with a mean of 90 tests/lO cm3 (Korsun et 3). The dominant On the similar to sandy and muddy sediments of the open Tuble 5 . A comparison of mean greatest diameter of Cussidulinu reniforme test in glacimarine and marine sediments. x - diameter, SE - standard error. n - number of tests Table 6. Number of calcareous foraminifera in grab and core samples from two sites in Nordensheld Bay, Novaja Zemlja (tests per 100 g dry sediment) Station x (pm) SE n General Location Marine sediments 67 1 206.7 8.0 30 W Barents Sea 666 203.4 7 . 8 22 W Barents Sea 396 194.4 5.4 40 W Barents Sea Glacimarine sediments Ho-2 147.9 8.6 24 Hornsund. W Spitsbergen 894 168.5 6.8 50 Nordensheld Bay, N.Z. 895 161.4 1 1 3 22 Nordensheld Bay, N.Z. Station 894 895 Grab (0-1 cm) Total 200 8 Live 63 % 17% mean ? SE 282 5 100 54 2 13 min 78 13 max 891 15 1 Core core top (0-5 cm) 891 52 28 S. A . Korsun e t a l . DIAMETER, prn 671 6 6 6 396 H o - 2 8 9 4 895 STATION big. I 1 hlean greatest diamctsr of the C'assiduhiio renifonnr test i n g l ~ i o m a r i n e and marine sediments. Bar = Y j c i con- fidence intc'rval al. 1994). In contrast, the biomass in the middle of Nordensheld Bay (0.03mg/10cm3) is two orders of magnitude less than the biomass in adjacent areas of the sea (Fig. 12). T h e larger (> 1 m m ) arenaceous foraminifera such as Rhab- dammina abyssorrcm (Sars, 1868). Hypperammina subnodosa, Pelosina uariabilis are common in muddy Barents Sea sediments and constitute the majority, ca. 9 0 7 ~ . of t h e foraminiferal biomass (Korsun e t al. 1994). Such larger species or any foraminifera >0.250 mm in diameter are not 0 5 F 5 0 2 0 0 L . 2 0 2 5 4 - 0 1 5 0 10 0 05 0 found in Nordensheld Bay. D u e t o the smaller test size, t h e foraminiferal biomass is significantly lower in Nordensheld Bay t h a n in t h e open Bar- ents S e a though the number of live specimens is similar (Fig. 12). Macrofauna biomass is low (< 1 g/m?) in glacier-proximal sediments with seasonal lami- nations in Hornsund (Gorlich et al. 1987). T h e laminations indicate the absence of bioturbation and hence. an inhibited macrobenthos (Giirlich et al. 1987). W e infer that foraminiferal biomass shows a similar decrease in Nordensheld Bay, Novaja Zemlja. Foraminiferol test size T h e analysis of foraminifera from Novaja Zemlja and Svalbard fjords shows test size diminishing in t h e glaciomarine sediments compared to marine sediments from the open Barents Sea. In the glaciomarine sediments of Nordensheld Bay. for- aminiferal tests a r e absent in sieve fractions >0.25 mm. In contrast, all of thirty-six for- aminiferal samples from the open Barents Sea have a number of specimens larger than 1 mm (Korsun 1991). The studied cores show smaller test size from glaciomarine sediments, indicative of juvenile specimens. A high occurrence (up to 5 0 7 r ) of these small foraminifera has not been observed in Holocene sequences from the open Barents Sea ( 0 s t b y & Nagy 1982; Korsun et al. 1994; among others). T h e high frequency of juv- enile tests indicates a high mortality in the fossil populations. Feyling-Hanssen (1982) noted that BARENTSSEA NORDENSHELD BAY 4 + 4 c 2 0 BIOMASS ' SIZE 1 CLASS v1 rl mrn C 0 5 - 1 : 0 25-0 5 FORAMINIFERA 646 653 896 87 4 894 895 S T A T ION 1 5 0 125 n 100 $ - \ v) 7 5 5 a 2 50 foraminiferal biomass Fig. 1 2 . Sizc distribution of (cytoplasmic volume) and number of live foraminifera 25 in Nordensheld Bay. Novaja Zemlja. Two 0 samples from the northeastern Barents Sea are shown for comparison. Recent foraminifera in glrcioniarine sediments 29 E . clavatztm specimens from glacial deposits are smaller in comparison to tests from full marine environments. Our results show that the other foraminifera, typical of glaciomarine settings, C. reniforme (Osterman & Nelson 1989), demon- strate a similar tendency and the difference is highly significant. The linear size of C. reniforme tests in glaciomarine sediments of Nordensheld Bay (Novaja Zemlja) and Hornsund (Spitsber- gen) is 20% smaller than in marine sediments of the open Barents Sea. We presume that the smaller size of fora- minifera in the glaciomarine sediments is an example of the opportunistic response to an environmental stress. In fjords influenced by gla- cier discharge, the inferred environmental par- ameters affecting benthic populations are meltwater discharge and high sedimentation rates (Appolonio 1973; Pierson 1980; Gdrlich et al. 1987). Intrusion of particulate rich meltwater into the bottom part of the water column is uncommon in glaciomarine environments (Gilbert 1983). Meltwater usually occupies the upper part of the water column and indirectly effects benthos com- munities via diminishing the primary production in the plankton community, that reduces organic flux to the bottom (Gorlich et al. 1987). We favour high sedimentation rates as the dominant controlling factor for diminishing foraminiferal test size. Rapid settling of sediment and turbidite deposition may continuously disturb benthos communities burying the fauna and maintain the benthos community at an early stage of the suc- cession. Such pioneer communities are charac- terised by high mortality of immature specimens and typically consist of opportunistic species which have a small size and a short life cycle (Odum 1971). The foraminiferal test size decreasing in the studied glaciomarine sediments versus the full marine sediments in the open Barents Sea is expressed in the absence of larger species, paucity of large specimens, and high occurrence for juv- enile foraminifera. This difference may be useful as another indicator of glaciomarine settings in paleoreconstructions. Rare species The foraminiferal fauna in the studied glacio- marine sediments (Table 2) is represented mostly by taxa characteristic of the Arctic zoogeographic province of the Barents Sea (Digas 1970). There are two species whose presence is quite unusual for the Barents Sea region, P. niveuin and Q. stalkeri. We found the first species, P. niueum, in both cores from Nordensheld Bay but not in the mod- ern samples. 'This species has not been registered in the surface sediments of the open Barents Sea (Digas 1970; Steinsund et al. in press). Several tests (unstained) have been observed in the inner part of Yarnyshnaya Bay, Kola Peninsula, 69"07'N, 36"03'E (Korsun 1986). Live specimens of this foraminifera are only found in two shallow water sites at 4 and 1 2 m on Franz Josef Land (Korsun unpubl. data). The limited occurrence of this species precludes an environmental inter- pretation. Q. stalkeri is present in the modern samples and in all the cores except for Ho-2. It is a sub- dominant or dominant species in several samples (Figs. 7 , 9, and 10). This species is quite rare in the open Barents Sea. In the total calcareous foraminiferal data set for the Barents and Kara Seas (598 samples; Steinsund et al. in press), Q. stalkeri occurs (about 1%) only in 10 samples from the open Sea. No live specimen of this species is found in sixty samples from the open Barents Sea (Korsun et al. 1994). Q. stalkeri has been registered neither in the Kola Peninsula Bays (Schedrina 1958: Korsun 1986,1992) nor in Franz Josef Land (Basov 1961; Lukina 1977). In contrast, Q. stalkeri is common in surface sediments from Svalbard fjords (Nagy 1965; E l v e r h ~ i et al. 1980). This species, including live specimens, was identified in six fjords on western and northern Spitsbergen and composed up to 14% of the total fauna (Hald & Korsun, unpubl.). Although, Q. stalkeri has been supposedly found in a variety of near-shore environments (Feyling-Hanssen et al. 1971), the occurrence of the species in the Barents Sea region seems to have some connection to modern fjord environ- ments of Novaja Zemlja and Svalbard. Q. stalkeri is possibly an indicator of glaciomarine depo- sitional environments. Conclusion N . labradorica and I. norcrossi reach peak abun- dance in the outer fjord samples. C. reniforme and Allogromiina spp. dominate foraminifera in the middle and inner fjord, closer to the glacier outlet. The foraminiferal dis- 30 S . A . Korsun et al. tribution and changing dominance of species in Nordensheld Bay is similar t o Svalbard fjords that are affected by glacial discharge. Ecological stress is probably caused by the high and changeable sedimentation rate and meltwater flux (c.f. Gor- lich e t al. 1987). Q. stalkeri is frequent in Novaja Zemlja and Svalbard fjords compared to the other areas of the Barents Sea region as a possible indicator of glaciomarine settings. In Nordensheld Bay, the number of live fora- minifera in the outer and middle fjord (24-122 spec./lO cm3) is similar t o the values from the open Barents Sea, whereas the biomass (0.03 mg/ 10 cm3) is two orders of magnitude less d u e to a smaller test size. Tests of C. reniforme are significantly smaller in glaciomarine sediments than in marine sedi- ments in t h e Barents Sea. Glaciomarine sedi- ments have in general a noticeable lack of large tests and species and an abundance of juveniles. The smaller test size is an opportunistic response of the foraminiferal populations to the environ- mental stress of glacier proximity. Ackiiowledgemenrs. - G . A. Tarasov supplied cores from Bellsund and Hornsund fjords Early reviews by G . G . Matishov. P.-I. Steinsund. M. Hald. J Snvder. P N. Webb. A . Reed and D . Rodbell were helpful in focusing the discussion. C. Hart and J . Snyder absisted with translation. We gratcfull? acknowledge the captains and crewt of the R V D A L h l E ZELENTS? and R \ POMOR for probiding a reliable sampling platform. This research w a s partially supported by the U . S . National Science Foundation Grant DPP-W)1471 and the Office of Naval Research Contract N00014-97-1908. We appreciate the draftman\hip of J . Nag! and word-processing assistance of S J . Harrk. This i s BPRC contribution #948. References Aksyonov. A . A . (ed.) 1987: The A r c f i c s h e l f o f Eurasia during rhe Lore Qitareriiary. Nauka. Moscow. 278 pp. (In Russian). Appolonio. S. 1973: Glaciers and nutrients in Arctic beas. Science 1XO. 491-49.2 Basov. V A . 1961: Composition and distribution of fora- minifcr;i in sediments from Franz Josef Land. liuclx N I l C A I 2 4 . 61-h5. ( I n Russian) Boulton. 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